THE  UNIVERSITY 


OF  ILLINOIS  ^ - 
LIBRARY 


557 

Xb  r 
no.62~  65. 


GB°tOsy; 


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THE 


MISCELLANEOUS  DOCUMENTS 

OP  THE 

HOUSE  OF  REPRESENTATIVES 

FOR  THE 


SECOND  SESSION  OF  THE  FIFTY-FIRST  CONGRESS. 

18  9 0-’91. 

WITH  INDEX. 


IN  SIXTEEN  VOLUMES. 


WASHINGTON: 

GOVERNMENT  PRINTING  OFFICE. 
1891. 


I 


6 5 7 
Xfc> 

h'  0 & -i,  - (p  ^ 


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vV 


557 


X*= 

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INDEX  TO  HOUSE  MISCELLANEOUS  DOCUMENTS. 


CONTENTS  OF  THE  VOLUMES. 


Vol.  l..Nos.  1 to  127,  inclusive,  except  Nos.  12, 13, 
14,  76, 77,78,108.- 
Vol.  2.. No.  12. 

Vol.  3.. No.  13. 

Vol.  4.. No.  14. 

Vol.  5.. No.  76. 

Vol.  6.. No.  77. 

Vol.  7.. No.  78.  • 

Vol.  8.. No.  108, 133,134,135 


Vol.  9.. No.  128. 

Vol.  10.. No.  129,  pt.  1. 
Vol.  11..  No.  129,  pt.  2. 
Vol.  12..  No.  130. 

Vol.  13..  No.  131. 

Vol.  14..  No.  132. 

Vol.  15..  No.  136. 

Vol.  16..  No.  137. 


Subjects. 


No. 


Vol. 


A. 


Alexander,  John  W.,  administrator,  report  of  Court  of  Claimson  case  of. 

Anacostia  and  Potomac  River  Railroad,  annual  report  of 

Army,  retired  officers,  resolution  relative  to  in  the  civil  service 

Astronomical  observations  for  1886 

Ayres,  Asa  B.,  et  al.,  resolution  to  refer  claims  to  Court  of  Claims 


121 

84 

92 

132 

120 


B. 


Bailey,  John  C.,  administrator, report  of  Court  of  Claims  on  case  of... 

Barnett,  J.  C.,  administrator,  report,  of  Court  of  Claims  on  case  of 

Barnett,  Julia,  resolution  to  refer  claim  to  Court  of  Claims 

Beachley,  Ezra  and  Jonas,  executors,  report  of  Court  of  Claims  on  case 

of 

Boarman,  Aleck,  resolution  to  impeach  

Brashear,  Martha,  administratrix,  report  of  Court  of  Claims  on  case  of. 

Brown,  F.  W.,  administrator,  report  of  Court  of  Claims  on  case  of 

Bruen,  Capt.  John  T.,  resolution  to  refer  claim  to  Court  of  Claims 


118 

71 

90 

51 

117 

97 
16 

98 


C. 


Calhoon,  Clement,  report  of  Court  of  Claims  on  case  of 

Canter,  Isaac  W.,  administrator,  report  of  Court  of  Claims  on  case  of  .. 
Capitol,  North  O street  and  South  Washington  Railroad  Company,  an- 
nual report  of 

Caruth,  Thomas,  report  of  Court  of  Claims  on  case  of 

Chapin,  Virginius  P.,  report  of  Court  of  Claims  on  case  of 

Chapman,  William  H.,  report  of  Court  of  Claims  on  case  of 

Christian  Church,  of  Marshall,  Mo.,  resolution  to  refer  claim  to  Court  of 

Claims 

Claims,  report  of  Treasury  Department  in  relation  to  certain  specified 

in  House  Ex.  Doc.  No.  314,  Fifty-first  Congress,  first  session 

Clark,  Samuel  I.,  assignee,  report  of  Court  of  Claims  on  case  of 

Clem,  Anderson  A.,  report  of  Court  of  Claims  on  case  of 

Clerk  of  the  House  of  Representatives : 

Annual  report  of  the  clerks  and  employes  in  the  House 

Report  on  inventory  of  public  property  in  possession  of 

Commissioner  of  Fish  and  Fisheries,  expenditures  by  the 

Congressional  Library,  report  on  construction  of  building  for  the 

Conrad,  Ebenezer  J.  et  al.,  report  of  Court  of  Claims  on  case  of 

Conrad,  John  D.,  report  of  Court  of  Claims  on  case  of 


21 

62 

95 

60 

81 

42 

126 

22 

65 

67 

6 

10 

5 

4 

17 

28 

in 


1 

1 

1 

14 

1 


l 

1 

1 

1 

1 

1 

1 

1 


1 

1 

1 

1 

l 

•1 

1 

1 

1 

1 

1 

1 

1 

1 

1 

1 


N0\6  \ 


IV 


INDEX  TO  HOUSE  MISCELLANEOUS  DOCUMENTS. 


Subject. 


Constitution  of  the  United  States,  relating  to  violation  of  the  four- 
teenth amendment  to  the 

Consular  reports 

Contested-election  cases,  digest  of 

Contested-election  cases,  print  digest  of,  in  the  Fifty-first  Congress  ... 
Court  of  Claims : 

Report  of  the,  on  judgments  of  the - 

Report  of  dismissed  cases  by  the 

Creek  Indians,  protest  of  delegates  of  the,  in  relation  to  jurisdiction  of 

Federal  courts  in  Indian  Territory 

Crockett,  John  T.,  report  of  Court  of  Claims  on  case  of 


No. 


Vol. 


122  1 

128  9 

137  16 

105  1 


11  1 

40  1 


104  1 

45  1 


D. 


Daub,  Ezra,  report  of  Court  of  Claims  on  case  of 

Deck,  George,  report  of  Court  of  Claims  on  case  of 

De  Loach,  Claiborne,  estate  of,  resolution  to  refer  claim  to  Court  of 

Claims 

Department  of  Labor,  expenditures  in  the 

District  of  Columbia,  Zoological  Park  Commission,  final  report  of 

Donato,  Relate  A.  et  al.,  resolution  to  refer  claims  to  Court  of  Claims. . 
Doorkeeper,  House  of  Representatives  : 

Report  of  property  in  possession  of..... 

Report  of  sale  of  waste  paper 


24 

54 

101 

9 

93 

115 


8 


1 

1 

1 

1 

1 

1 

1 

1 


E. 


Eckington  and  Soldiers’  Home  Railway  Company,  annual  report  of 

Elkins,  William  A.,  report  of  Court  of  Claims  on  case  of 

Ely,  Robert  M.  et  al.,  resolution  to  refer  claims  to  Court  of  Claims 

Embry.  W.  J.,  executor,  report  of  Court  of  Claims  on  case  of 


85 

48 

106 

64 


F. 


Fairex,  Mathilde  M.,  administratrix,  report  of  Court  of  Claims  on 

case  of.. 

Fish  Bulletin,  report  for  1889 

Fish  and  Fisheries,  report  of  the  Commissioner  of,  on  expenditures 

Fish  hatchery,  resolution  relative  to,  in  northern  New  York... 

Fisher,  Isaac,  et  al.,  resolution  to  refer  claims  of  to  Court  of  Claims  .... 

Fisher,  John,  et  al.,  resolution  to  refer  claims  to  Court  of  Claims 

Flagg,  Robert  S.  and  Thomas  G.,  executors,  report  of  Court  of  Claims 

on  case  of 

Flower,  Mary  J.,  report  of  Court  of  Claims  on  case  of 

Fort  Brown  military  reservation,  relation  to  rent  of 

Freedmans’  Savings  and  Trust  Company,  annual  report  of  the  commis- 
sioner for  1890  


35 

131 

5 

46 

110 

113 

61 

59 

100 

26 


G. 


Galloway,  Thomas  S.,  administrator,  report  of  Court  of  Claims  on  case 

of 

Gay,  Hon,  Edward  J.,  deceased,  eulogies  upou 

Geological  Survey,  bulletons  62  to  65 

Georgetown  Barge,  Dock,  Elevator  and  Railway  Company,  report  of 

names  of  stockholders  and  condition  of 

Georgetown  and  Tennallytown  Railway  Company,  annual  report  of.. 
Gillilan,  Ruth  S.,  administratrix,  report  of  Court  of  Claims  onoase  of.. 

Gray,  George  L.,  report  of  Court  of  Claims  on  case  of 

- i • 

H. 


37 

108 

136 

87 

86 

63 

79 


Heberlein,  August,  estate  of,  resolution  to  refer  claim  to  Court  of 

Claims  

Hightower,  Thomas,  report  of  Court  of  Claims  on  'case  of.. 

Horse  Diseases,  report  relating  to 


107 

66 

130 


1 

1 

1 

1 


1 

13 

1 

1 

1 

1 

1 

1 

1 

1 


1 

8 

15 

1 

1 

1 

1 


1 

1 

12 


INDEX  TO  HOUSE  MISCELLANEOUS  DOCUMENTS. 


V 


Subject. 


No. 


House  of  Representatives : 

Clerk  of  (Hon.  Edward  McPherson),  annual  report  of  clerks  and 

employ 6 of  the 

report  on  public  property  in  pos- 
session of 

Committees,  list  of  standing  and  select 

Doorkeeper,  report  of  property, 

report  of  sale  of  waste  paper 

Galleries  of  the,  removal  of  partition  and,  on  the  south  side  of 

Members,  list  of .. 

alphabetical  list  of i 

Special  messengers,  resolution  to  pay 

Ho wery,  Lewis,  report  of  Court  of  Claims  on  case  of 


6 

10 

2 

7 

8 

125 

1 

3 

72 

57 


I. 


Indian  Territory,  protest  of  Creek  delegates  against  bill  extending 
jurisdiction  of  Federal  courts  in 

J. 

Jews  in  Russia,  relative  to 

K. 

Keedy,  C.  M.,  George  W.,  and  Samuel  J.,  executors,  report  of  Court  of 
Claims  on  case  of 


104 


103 


75 


L. 

Library  of  Congress,  report  on  construction  of  building  for 
Lilly,  Elijah,  report  of  Court  of  Claims  on  case  of  

M. 


4 

33 


Manson,  William  T.,  report  of  Court  of  Claims  on  case  of 

Martin,  Edmund  H.,  heirs  of,  report  of  Court  of  Claims  on  case  of 

Meaher  & Meaher,  resolution  to  refer  claim  to  Court  of  Claims 

Merrifield,  Samuel  B.,  report  of  Court  of  Claims  on  case  of 

Mississippi  River,  levees  of  the 

Mullendore,  Daniel  M.,  report  of  Court  of  Claims  on  case  of 

N. 


30 

43 

114 

123 

127 

25 


National  Home  for  Disabled  Volunteer  Soldiers,  report  of  the  Board  of 

Managers  of  the,  for  1890 

Neidlinger,  Samuel,  estate  of,  report  of  Court  of  Claims  on  case  of 

New  Mexico,  the  secretary  of,  letter  from  the,  in  relation  to  Spanish 

land-grant  court J 

New  York,  resolution  relative  to  fish  hatchery  in  northern 

Nichols,  Henry  C.,  report  of  Court  of  Claims  on  case  of 

Norton,  Sarah  E.,  report  of  Court  of  Claims  on  case  of 

Nutt,  Julia  A.,  executrix,  report  of  Court  of  Claims  on  case  of 


38 

44 

96 

46 
119 

47 
82 


P. 


Peacock,  Martha  A.,  report  of  Court  of  Claims  on  case  of.... 

Phelan,  Hon.  James,  eulogies  upon 

Phetzing  Cornelius,  resolution  to  refer  claim  of,  to  Court  of  Claims 

Pierson,  Charles  A.,  et  aZ.,  resolution  to  reler  claims  to  Court  of  Claims. 

Ponder,  W.  M.,  administrator,  report  of  Court  of  Claims  on  case  of 

Pope,  Henry  L.,  report  of  Court  of  Claims  on  case  of 

Public  property : 

Report  of  Clerk  of  House  of  Representatives  on,  in  possession  of. 
Report  of  Doorkeeper,  House  of  Representatives  on  sale  of  waste 
paper 


53 

135 

116 

111 

55 

94 

10 

8 


Vol. 


1 

1 

1 

1 

1 

1 

1 

1 

1 

1 


1 


1 


1 


1 

1 


1 

1 

1 

1 

1 

1 


1 

1 

1 

1 

1 

1 

1 


1 

8 

1 

1 

1 

1 

1 

I 


VI 


INDEX  TO  HOUSE  MISCELLANEOUS  DOCUMENTS. 


Subject. 


No. 


Public  Property — Continued. 

Report  of  Doorkeeper,  House  of  Representatives,  submitting  inven- 
tory of 


7 


Q. 


Quinn,  Robert,  report  of  Court  of  Claim  on  case  of. 

R. 


34 


Raiford,  Philip,  administrator,  report  of  Court'of  Claims  on  case  of 

Reformed  Church,  Sharpsburgh,  Md.,  report  of  Court  of  Claims  on  case 

of 

Rogers,  Samuel  E.,  report  of  Court  of  Claims  on  case  of 

Roulette,  William,  report  of  Court  of  Claims  on  case  of 

Russell,  James  B.,  report  of  Court  of  Claims  on  case  of 

Russia,  relative  to  Jews  in 


18 

32 

29 

68 

124 

103 


S. 


Saffold,  Mary  E.,  report  of  Court  of  Claims  on  case  of 

Secretary  of  War,  resolution  requesting  the,  to  furnish  information 

relative  to  retired  army  officers  in  the  civil  service 

Sitting  Bull,  Chief,  resolution  relative  to  arrest  and  killing  of 

Skaggs,  Ewing  M.,  estate  of,  report  of  Court  of  Claims  on  case  of 

Smith,  Grafton  F.,  administrator,  report  of  Court  of  Claims  on  case  of. 

Smithsonian  Institution,  report  of  expenditures  of  the 

Smithsonian  Institution,  annual  repert  for  1890 

South,  William  B.,  executor,  report  of  Court  of  Claims  on  case  of 

Spanish  land-grant  court,  letter  from  the  secretary  of  New  Mexico  in 

relation  to 

Special  messengers,  House  of  Representatives,  resolution  for  appro- 
priation to  pay  salary  of 

Spencer,  C.  O.,  report  of  Court  of  Claims  on  case  of 

Stone,  Jeff.  M.,  report  of  Court  of  Claims  on  case  of 

Stout,  Lindsay,  representatives  of,  resolution  to  refer  claim  to  Court  of 

Claims 

Swart,  Barnett  T.,  report  of  Court  of  Claims  on  case  of 


99 

92 

80 

73 
52 
39 

129 

36 

96 

72 

70 

50 

109 

74 


T. 


Tally,  J.  M.  administrator,  report  of  Court  of  Claims  on  case  of 

Thompson,  Abel  A.,  report  of  Court  of  Claims  on  case  of 

Tounoir,  Lucile,  administratrix,  report  of  Court  of  Claims  on  case  of.. . 
Treasury  Department,  report  of  Second  Comptroller  in  relation  to  cer- 
tain claims  included  in  House  Ex.  Doc.  No.  314  Fifty-first  Congress, 

first  session s 

Turner,  John,  report  of  Court  of  Claims  on  case  of 

Turnley,  Parmenus  T.,  report  of  Court  of  Claims  on  case  of 

Tweedy,  Robert  E.,  report  of  Court  of  Claims  on  case  of 


56 

102 

23 


22 

58 

19 

89 


V. 


Van  Camp,  Aaron,  report  of  Court  of  Claims  on  case  of 

Von  Balsan,  R.,  administrator,  report  of  Court  of  Claims  on  case  of 

Voters.  (See  Constitution  of  the  United  States.) 

Vulture , Brig,  report  of  Court  of  Claims  on  case  of 


81 

27 

41 


W. 


Waddell,  Charlotte  A.,  executrix,  report  of  Court  of  Claims  on  case  of. 
War  of  the  Rebellion,  Official  Records  of: 

Series  1,  vol.  31,  part  1 - 

Series  1,  vol.  31,  part  2 

Series  1,  vol.  31,  part  3 

Series  1,  vol.  32,  part  1 


69 

12 

13 

14 
76 


Vol. 


1 


1 


1 

1 

1 

1 

1 

1 


1 

1 

1 

1 

1 

1 

10,11 

1 

1 

1 

1 

1 

1 

1 


1 

1 

1 


1 

1 

1 

1 


1 

1 

1 


1 


cn  rfi.  CO  to 


INDEX  TO  HOUSE  MISCELLANEOUS  DOCUMENTS. 


YII 


Subject. 


No. 


War  of  the  Rebellion,  Official  Records  of — Continued. 

Series  1,  vol.  32,  part  2 

Series  1,  vol.  32,  part  3 

Washington  and  Georgetown  Railway  Company,  annual  report  of 

Walker,  Hon.  James,  eulogies  upon 

Watson,  Hon.  Lewis,  eulogies  upon 

Watson  Samuel  report  of  Court  of  Claims  on  case  of 

Western  Miama  Indians,  report  of  Court  of  Claims  on  case  of  

Wheeler,  William  B.,  executor,  report  of  Court  of  Claims  on  case  of 

Williams,  Mary  O.,  report  of  Court  of  Claims  on  case  of 

Woody ard,  Mathew,  report  of  Court  of  Claims  on  claim  of.... 


77 

78 
91 

134 

133 

15 

83 

49 

20 

88 


Y. 


Young,  Thomas  P.,  et  ah,  resolution  to  refer  claims  to  Court  of  Claims..  112 
Youngs,  Fannie,  and  Henrietta  G.,  executrics,  report  of  Court  of  Claims 
on  case  of 31 


Z. 


Zoological  Park  Commission,  final  report  of. 


93 


Vol. 


6 

7 

1 

8 
8 

1 

1 

1 

1 

1 


1 

1 


1 


51st  Congress,  > HOUSE  OF  REPRESENTATIVES,  t Mis.  Doc. 
2d  Session.  I (No.  136. 


DEPARTMENT  OF  THE  INTERIOR 


BULLETINS 


OF  THE 

UNITED  STATES 

GEOLOGICAL  SURVEY 


NT  os.  6*2  t o 65 


WASHINGTON 

GOVERNMENT  PRINTING  OFFICE 

1891 


Title  for  subject  entry.  Author  title.  Series  title. 


LIBRARY  CATALOGUE  SLIPS. 


United  States.  Department  of  the  interior.  ( U.  S.  geological  survey). 

Department  of  the  interior  } — ( Bulletin  j of  the  | United 
States  I geological  survey  | no.  62  | [Seal  of  the  department]  | 

Washington  | government  printing  office  | 1890 

Second  title:  United  States  geological  survey  | J.  W.  Powell, 
director  | — | The  greenstone  schist  areas  | of  the  | Menominee 
and  Marquette  regions  of  Michigan  | A contribution  to  the  sub- 
ject of  dynamic  metamorphism  | in  eruptive  rocks  j by  [ George 
Huntington  Williams  | with  an  introduction  by  | Roland  Duer 
Irving  | [Vignette]  | 

Washington  | government  printing  office  | 1890 

8°.  241pp.  16  pi. 


Williams  (George  Huntington). 

United  States  geological  survey  | J.  W.  Powell,  director  | — | 
The  greenstone  schist  areas  | of  the  | Menominee  and  Marquette 
regions  of  Michigan  | A contribution  to  the  subject  of  dynamic 
metamorphism  | in  eruptive  rocks  | by  | George  Huntington  Will- 
iams | with  an  introduction  by  | Roland  Duer  Irving  j [Vignette]  | 
Washington  | government  printing  office  | 1890 

8°.  241  pp.  16  pi. 

(United  States.  Department  of  the  interior.  (TJ.  S.  geological  survey). 

Bulletin  62]. 


United  States  geological  survey  | J.  W.  Powell,  director  | — | 
The  greenstone  schist  areas  | oi  the  | Menominee  and  Marquette 
regions  of  Michigan  | A contribution  to  the  subject  of  dynamic 
metamorphism  | in  eruptive  rocks  | by  | George  Huntington  Will- 
iams | with  an  introduction  by  | Roland  Duer  Irving  | [Vignette]  | 
Washington  | government  printing  office  | 1890 
6°.  241pp.  16  pi. 

(United  States.  Department  of  the  interior.  ( U.  S.  geological  survey). 
Bulletin  62]. 


ADVERTISEMENT. 


[Bulletin  No.  62.1 


The  publications  of  the  United  States  Geological  Survey  are  issued  in  accordance  with  the  statute 
approved  March  3,  1879,  which  declares  that— 

“Thepublicationsof  theGeological  Survey  shall  consistof  the  annual  report  of  operations,  geological 
and  economic  maps  illustrating  the  resources  and  classification  of  the  lands,  and  reports  upon  general 
and  economic  geology  and  paleontology.  The  annual  report  of  operations  of  the  Geological  Survey 
shall  accompany  the  annual  report  of  the  Secretary  of  the  Interior.  All  special  memoirs  and  reports 
of  said  Survey  shall  be  issued  in  uniform  quarto  series  if  deemed  necessary  by  the  Director,  but  other- 
wise in  ordinary  octavos.  Three  thousand  copies  of  each  shall  be  published  for  scientific  exchanges 
and  for  sale  at  the  price  of  publication ; and  all  literary  and  cartographic  materials  received  in  exchange 
shall  be  the  property  of  the  United  States  and  form  a part  of  the  library  of  the  organization : And  the 
money  resulting  from  the  sale  of  such  publications  shall  be  covered  into  the  Treasury  of  the  United 
States.” 

On  July  7,  1882,  the  following  joint  resolution,  referring  to  all  Government  publications,  was  passed 
by  Congress: 

‘ ‘ That  whenever  any  document  or  report  shall  be  ordered  printed  by  Congress,  there  shall  be  printed, 
in  addition  to  the  number  in  each  case  stated,  the  ‘ usual  number  ’ (1,900)  of  copies  for  binding  and 
distribution  among  those  entitled  to  receive  them.” 

Except  in  those  cases  in  which  an  extra  number  of  any  publication  has  been  supplied  to  the  Survey 
by  special  resolution  of  Congress  or  has  been  ordered  by  the  Secretary  of  the  Interior,  this  office  has 
no  copies  for  gratuitous  distribution. 

ANNUAL  REPORTS. 

I.  First  Annual  Report  of  the  United  States  Geological  Survey,  by  Clarence  King.  880.  8°.  79  pp. 
1 map.— A preliminary  report  describing  plan  of  organization  and  publications. 

II.  Second  Annual  Report  of  the  United  States  Geological  Survey,  1880- '81,  by  J.  W.  Powell.  1882. 
8°.  lv,  588  pp.  62  pi.  1 map. 

III.  Third  Annual  Report  of  the  United  States  Geological  Survey,  1881-82,  by  J.  W.  Powell.  1883. 
8°.  xviii,  564  pp.  67  pi.  and  maps. 

IV.  Fourth  Annual  Report  of  the  United  States  Geological  Survey,  1882-83,  by  J.  W.  Powell.  1884. 
8°.  xxxii,  473  pp.  85  pi.  and  maps. 

V.  Fifth  Annual  Report  of  the  United  States  Geological  Survey,  1883-84,  by  J.  W.  Powell.  1885. 
8°.  xxxvi,  469  pp.  58  pi.  and  maps. 

VI.  Sixth  Annual  Report  of  the  United  States  Geological  Survey,  1884-’85,  by  J.  W.  Powell.  1885. 
8°.  xxix,  570  pp.  65  pi.  and  maps. 

VII.  Seventh  Annual  ReportoftheUnitedStatesGeologicalSurvey,  1885-86,  by  J.  W.  Powell.  1888. 
8°.  xx,  656  pp.  71  pL  and  maps. 

VIII.  Eighth  Annual  Report  of  the  United  States  Geological  Survey,  1886— ’87,  by  J.  W.  Powell.  1889. 
8°.  2 v.  xix,  474,  xii  pp.  53  pi.  and  maps ; 1 p.  1. 475-1063  pp.  54-76  pi.  and  maps. 

IX.  Ninth  Annual  Report  of  the  United  States  Geological  Survey,  1887-88,  by  J.  W.  Powell.  1890. 
8°.  xiii,  717  pp.  88  pi.  and  maps. 

The  Tenth  Annual  Report  is  in  press. 


MONOGRAPHS. 

I.  Lake  Bonneville,  by  Grove  Karl  Gilbert.  1890.  4°.  xx,  438  pp.  51  pi.  1 map.  Price  $1.50. 

II.  Tertiary  History  of  the  Grand  Canon  District,  with  atlas,  by  Clarence  E.  Dutton,  Capt.  IJ.  S.  A. 
1882.  4°.  xiv,  264  pp.  42  pi.  and  atlas  of  24  sheets  folio.  Price  $10.12. 

III.  Geology  of  the  Comstock  Lode  and  the  Washoe  District,  with  atlas,  by  George  F.  Becker.  1882. 
4°.  xv,  422  pp.  7 pi.  and  atlas  of  21  sheets  folio.  Price  $11.00. 

IV.  Comstock  Mining  and  Miners,  by  Eliot  Lord.  1883.  4°.  xiv,  451  pp.  3 pi.  Price  $1.50. 

V.  The  Copper-Bearing  Rocks  of  Lake  Superior,  by  Roland  Duer  Irving.  1883.  4°.  xvi,  464  pp. 
15  1.  29  pi.  and  maps.  Price  $1.85. 

VI.  Contributions  to  the  Knowledge  of  the  Older  Mesozoic  Flora  of  Virginia,  by  William  Morris 
Fontaine.  1883.  4°.  xi,  144  pp.  54  1.  54  pi.  Price  $1.05. 


II 


ADVERTISEMENT. 


VO.  Silver-Lead  Deposits  of  Eureka,  Nevada,  by  Joseph  Story  Curtis.  1884  . 4°.  xiii,  200  pp.  16 
pi.  Price  $1.20. 

Vin.  Paleontology  of  the  Eureka  District,  by  Charles  Doolittle  Walcott.  1884.  4°.  xiii,  298  pp. 
241.  24  pi.  Price  $1.10. 

IX.  Bracliiopoda  and  Lamellibranchiata  of  the  Raritan.  Clays  and  Greensand  Marls  of  New  Jersey 
by  Robert  P.  Whitfield.  1885.  4°.  xx,  338  pp.  35  pi.  1 map.  Price  $1.15. 

X.  Dinocerata.  A Monograph  of  an  Extinct  Order  of  Gigantic  Mammals,  by  Othniel  Charles  Marsh. 
1886.  4°.  xviii,  243  pp.  561.  56  pi.  Price  $2.70. 

XI.  Geological  History  of  Lake  Lahontan,  a Quaternary  Lake  of  Northwestern  Nevada,  by  Israel 
Cook  Russell.  1885.  4°.  xiv,  288  pp.  46  pi.  and  maps.  Price  $1.75. 

XII.  Geology  and  Mining  Industry  of  Leadville,  Colorado,  with  atlas,  by  Samuel  Franklin  Emmons. 
1886.  4°.  xxix,  770  pp.  45  pi.  and  atlas  of  35  sheets  folio.  Price  $8.40. 

XIII.  Geology  of  the  Quicksilver  Deposits  of  the  Pacific  Slope,  with  atlas,  by  George  F.  Becker. 
1888.  4°.  xix,  486  pp.  7 pi.  and  atlas  of  14  sheets  folio.  Price  $2.00. 

XIV.  Fossil  Fishes  and  Fossil  Plants  of  the  Triassic  Rocks  of  New  Jersey  and  the  Connecticut  Val- 
ley, by  John  S.  Newberry.  1888.  4°.  xiv,  152  pp.  26  pi.  Price  $1.00. 

XV.  The  Potomac  or  Younger  Mesozoic  Flora,  by  William  Morris  Fontaine.  1889.  4°.  xiv,  377 
pp.  186  pi.  Text  and  plates  bound  separately.  Price  $2.50. 

XVI.  The  Paleozoic  Fishes  of  North  America,  by  John  Strong  Newberry.  1889.  4°.  340  pp.  53  pi. 
Price  $1.00. 

In  preparation  : 

— Gasteropoda  of  the  New  Jersey  Cretaceous  and  Eocene  Marls,  by  R.  P.  Whitfield. 

— The  Penokee  Iron-Bearing  Series  of  Northern  Wisconsin  and  Michigan,  by  Roland  D.  Irving  and 
C.  R.  Van  Hise. 

— Mollusca  and  Crustacea  of  the  Miocene  Formations  of  New  Jersey,  by  R.  P.  Whitfield. 

— Description  of  New  Fossil  Plants  from  the  Dakota  Group,  by  Leo  Lesquereux. 

— Geology  of  the  Eureka  Mining  District,  Nevada,  with  atlas,  by  Arnold  Hague. 

— Sauropoda,  by  O.  C.  Marsh. 

— Stegosauria,  by  O.  C.  Marsh. 

— Brontotheridae,  by  O.  C.  Marsh. 

— Report  on  the  Denver  Coal  Basin,  by  S.  F.  Emmons. 

— Report  on  Silver  Cliff  and  Ten-Mile  Mining  Districts,  Colorado,  by  S.  F.  Emmons. 

— Flora  of  the  Dakota  Group,  by  J.  S.  Newberry. 

— The  Glacial  Lake  Agassiz,  by  Warren  Upham. 

— Geology  of  the  Potomac  Formation  in  Virginia,  by  W.  M.  Fontaine. 

BULLETINS. 

1.  On  Hypersthene- Andesite  and  on  Triclinic  Pyroxene  in  Augitic  Rocks,  by  Whitman  Cross,  with  a 
Geological  Sketch  of  Buffalo  Peaks,  Colorado,  by  S.  F.  Emmons.  1883.  8°.  42pp.  "2  pi.  Price  10  cents. 

2.  Gold  and  Silver  Conversion  Tables,  giving  the  coining  values  of  troy  ounces  of  fine  metal,  etc.,  com- 
puted by  Albert  Williams,  jr.  1883.  8°.  8 pp.  Price  5 cents. 

3.  On  the  Fossil  Faunas  of  the  Upper  Devonian,  along  the  meridian  of  76°  30',  from  Tompkins  County 
N.  Y.,  to  Bradford  County,  Pa.,  by  Henry  S.  Williams.  1884.  8°.  36  pp.  Price  5 cents. 

4.  On  Mesozoic  Fossils,  by  Charles  A.  White.  1884.  8°.  36  pp.  9 pi.  Price  5 cents. 

5.  A Dictionary  of  Altitudes  in  the  United  States,  compiled  by  Henry  Gannett.  1884.  8°.  325  pp. 
Price  20  cents. 

6.  Elevations  in  the  Dominion  of  Canada,  by  J.  W.  Spencer.  1884.  8°.  43  pp.  Price  5 cents. 

7.  Mapoteca  Geologica  Americana.  A Catalogue  of  Geological  Maps  of  America  (North  and  South), 
1752-1881,  in  geographic  and  chronologic  order,  by  Jules  Marcou  and  John  Belknap  Marcou.  1884. 
8°.  184  pp.  Price  10  cents. 

8.  On  Secondary  Enlargements  of  Mineral  Fragments  in  Certain  Rocks,  by  R.  D.  Irving  and  C.  R. 
Van  Hise.  1884.  8°.  56  pp.  6 pi.  Price  10  cents. 

9.  AReport  of  work  done  in  the  Washington  Laboratory  during  the  fiscal  year  1883-84.  F.  W.  Clarke, 
chief  chemist.  T.  M.  Chatard,  assistant  chemist.  1884.  8°.  40  pp.  Price  5 cents. 

10.  On  the  Cambrian  Faunas  of  North  America.  Preliminary  studies,  by  Charles  Doolittle  Walcott. 
1884.  8°.  74  pp.  10  pi.  Price  5 cents. 

11.  On  the  Quaternary  and  Recent  Mollusca  of  the  Great  Basin ; with  Descriptions  of  New  Forms,  by 
R.  Ellsworth  Call.  Introduced  by  a sketch  of  the  Quaternary  Lakes  of  the  Great  Basin,  by  G.  K. 
Gilbert.  1884.  -8°.  66  pp.  6 pi.  Price  5 cents. 

12.  A Crystallographic  Study  of  the  Thinolite  of  Lake  Lahontan,  by  Edward  S.  Dana.  1884.  8°. 
34  pp.  3 pi.  Price  5 cents. 

13.  Boundaries  of  the  United  States  and  of  the  several  States  and  Territories,  with  a Historical 
Sketch  of  the  Territorial  Changes,  by  Henry  Gannett.  1885.  8°.  135  pp.  Price  10  cents. 

14.  The  Electrical  and  Magnetic  Properties  of  the  Iron-Carburets.  by  Carl  Barus  and  Vincent 
Strouhal.  1885.  8°.  238  pp.  Price  15  cents. 

15.  On  the  Mesozoic  and  Cenozoic  Paleontology  of  California,  by  Charles  A.  White.  1885.  8°. 
33  pp.  Price  5 cents. 


ADVERTISEMENT. 


Ill 


16.  On  the  Higher  Devonian  Faunas  of  Ontario  County,  New  York,  by  JohnM.  Clarke.  1885.  8°. 

86  pp.  3 pi.  Price  5 cents. 

17.  On  the  Development  of  Crystallization  in  the  Igneous  Rocks  of  Washoe,  Nevada,  with  Notes  on 
the  Geology  of  the  District,  by  Arnold  Hague  and  Joseph  P.  Iddings.  1885.  8°.  44  pp.  Price  5 cents. 

18.  On  Marine  Eocene,  Fresh- water  Miocene,  and  other  Fossil  Mollusca  of  Western  North  America, 
by  Charles  A.  White.  1885.  8°.  26  pp.  3 pi.  Price  5 cents. 

19.  Notes  on  the  Stratigraphy  of  California,  by  George  F.  Becker.  1885.  8°.  28  pp.  Price  5 cents. 

20.  Contributions  to  the  Mineralogy  of  the  Rocky  Mountains,  by  Whitman  Cross  and  W.  F.  Hille- 
brand.  1885.  8°.  114  pp.  1 pi.  Price  10  cents. 

21.  The  Lignites  of  the  Great  Sioux  Reservation.  A Report  on  the  Region  between  the  Grand  and  Mo- 
reau Rivers,  Dakota,  by  Bailey  Willis.  1885.  8°.  16  pp.  5 pi.  Price  5 cents. 

22.  On  New  Cretaceous  Fossils  from  California,  by  Charles  A.  White.  1885.  8°.  25  pp.  5 pi.  Price 
5 cents. 

23.  Observations  on  the  Junction  between  the  Eastern  Sandstone  and  the  Keweenaw  Series  on 

Keweenaw  Point,  Lake  Superior,  by  R.  D.  Irving  and  T.  C.  Chamberlin.  1885.  8°.  124  pp.  17  pi. 

Price  15  cents. 

24.  List  of  Marine  Mollusca,  comprising  the  Quaternary  Fossils  and  recent  forms  from  American 
Localities  between  Cape  Hatteras  and  Cape  Roque,  including  the  Bermudas,  by  William  Healey  Dali. 
1885.  8°.  336  pp.  Price  25  cents. 

25.  The  Present  Technical  Condition  of  the  Steel  Industry  of  the  United  States,  by  Pbineas  Barnes. 
1885.  8°.  85  pp.  Price  10  cents. 

26.  Copper  Smelting,  by  Henry  M.  Howe.  1885.  8°.  107  pp.  Price  10  cents. 

27.  Report  of  work  done  in  the  Division  of  Chemistry  and  Physics,  mainly  during  the  fiscal  year 

1884- ’85.  1886.  8°.  80  pp.  Price  10  cents. 

28.  The  Gabbros  and  Associated  Hornblende  Rocks  occurring  in  the  Neighborhood  of  Baltimore,  Md. 
by  George  Huntington  Williams.  1886.  8°.  78  pp.  4 pi.  Price  10  cents. 

29.  On  the  Fresh-water  Invertebrates  of  the  North  American  Jurassic,  by  Charles  A.  White.  1886. 
8°.  41  pp.  4 pi.  Price  5 cents. 

30.  Second  Contribution  to  the  Studies  on  the  Cambrian  Faunas  of  North  America,  by  Charles  Doo- 
little Walcott.  1886.  8°.  369  pp.  33  pi.  Price  25  cents. 

31.  Systematic  Review  of  our  Present  Knowledge  of  Fossil  Insects,  including  Myriapods  and  Arach- 
nida,  by 'Samuel  Hubbard  Scudder.  1886.  8°.  128  pp.  Price  15  cents. 

32.  Lists  and  Analyses  of  the  Mineral  Springs  of  the  United  States ; a Preliminary  Study,  by  Albertf? 
C.  Peale.  1886.  8°.  235  pp.  Price  20  cents. 

33.  Notes  on  the  Geology  of  Northern  California,  by  J.  S.  Diller.  1886.  8°.  23  pp.  Price  5 cents. 

34.  On  the  relation  of  the  Laramie  Molluscan  Fauna  to  that  of  the  succeeding  Fresh-water  Eocene 
and  other  groups,  by  Charles  A.  White.  1886.  8°.  54  pp.  5 pi.  Price  10  cents. 

35.  Physical  Properties  of  the  Iron-Carburets,  by  Carl  Barus  and  Vincent  Strouhal.  1886.  8°.  62 
pp.  Price  10  cents. 

36.  Subsidence  of  Fine  Solid  Particles  in  Liquids,  by  Carl  Barus.  1886.  8°.  58  pp.  Price  10  cents. 

37.  Types  of  the  Laramie  Flora,  by  Lester  F.  W ard.  1887.  8°.  354  pp.  57  pi.  Price  25  cents. 

38.  Peridotite  of  Elliott  County,  Kentucky,  by  J.  S.  Diller.  1887.  8°.  31  pp.  1 pi.  Price  5 cents. 

39.  The  Upper  Beaches  and  Deltas  of  the  Glacial  Lake  Agassiz,  by  Warren  Upham.  1887.  8°.  84 
pp.  1 pi.  Price  10  cents. 

40.  Changes  in  River  Courses  in  Washington  Territory  due  to  Glaciation,  by  Bailey  Willis.  1887.  8°. 

10  pp.  4 pi.  Price  5 cents. 

41.  On  the  Fossil  Faunas  of  the  Upper  Devonian— the  Genesee  Section,  New  York,  by  Henry  S. 
Williams.  1887.  8°.  121  pp.  4 pi.  Price  15  cents. 

42.  Report  of  work  done  in  the  Division  of  Chemistry  and  Physics,  mainly  during  the  fiscal  year 

1885- ’86.  F.  W.  Clarke,  chief  chemist.  1887.  8°.  152  pp.  1 pi.  Price  15  cents. 

43.  Tortiary  and  Cretaceous  Strata  of  the  Tuscaloosa,  Tonibigbee,  and  Alabama  Rivers,  by  Eugene 

A.  Smith  and  Lawrence  C.  Johnson.  1887.  8°.  189  pp.  21  pi.  Price  15  cents. 

44.  Bibliography  of  North  American  Geology  for  1886,  by  Nelson  H.  Darton.  1887.  8°.  35  pp. 
Price  5 cents. 

45.  The  Present  Condition  of  Knowledge  of  the  Geology  of  Texas,  by  Robert  T.  Hill.  1887.  8°.  94 
pp.  Price  10  cents. 

46.  Nature  and  Origin  of  Deposits  of  Phosphate  of  Lime,  by  R,  A.  F.  Penrose,  jr.,  with  an  Introduc- 
tion by  N.  S.  Shaler.  1888.  8°.  143  pp.  Price  15  cents. 

47.  Analyses  of  Waters  of  the  Yellowstone  National  Park,  with  an  Account  of  the  Methods  of  Anal- 
syis  employed,  by  Frank  Austin  Gooch  and  James  Edward  Whitfield.  1888.  8°.  84  pp.  Price  10 

cents. 

48.  On  the  Form  and  Position  of  the  Sea  Level,  by  Robert  Simpson  Woodward.  1888.  8°.  88  pp. 

Price  10  cents. 

49.  Latitudes  and  Longitudes  of  Certain  Points  in  Missouri,  Kansas,  and  New  Mexico,  by  Robert 
Simpson  Woodward.  1889.  8°.  133  pp.  Price  15  cents. 

50.  Formulas  and  Tables  to  facilitate  the  Construction  and  Use  of  Maps,  by  Robert  Simnson  Wood-' 

ward.  1889.  8°.  124  pp.  Prico  15  cents 


IV 


ADVERTISEMENT. 


51.  On  Invertebrate  Fossils  from  the  Pacific  Coast,  by  Charles  Abiathar  White.  1889.  8°.  102  pp. 

14  pi.  Price  15  cents. 

52.  Subaerial  Decay  of  Rocks  and  Origin  of  the  Red  Color  of  Certain  Formations,  by  Israel  Cook 
Russell.  1889.  8°.  65  pp.  5 pi.  Price  10  cents. 

53.  The  Geology  of  Nantucket,  by  Nathaniel  Southgate  Shaler.  1889.  8°.  55  pp.  10  pi.  Price  10 
cents. 

54.  On  the  Thermo-Electric  Measurement  of  High  Temperatures,  by  Carl  Barus.  1889.  8°.  313  pp. 
incl.  1 pi.  11  pi.  Price  25  cents. 

55.  Report  of  work  done  in  the  Division  of  Chemistry  and  Physics,  mainly  during  the  fiscal  year 

1886- 87.  Frank  Wiggles  worth  Clarke,  chief  chemist.  1889.  8°.  96  pp.  Price  10  cents. 

56.  Fossil  Wood  and  Lignite  of  the  Potomac  Formation,  by  Frank  Hall  Knowlton.  1889.  8°.  72  pp. 
7 pi.  Price  10  cents. 

57.  A Geological  Reconnaissance  in  Southwestern  Kansas,  by  Robert  Hay.  1890.  8°.  49  pp.  2 pi. 
Price  5 cents. 

58.  The  Glacial  Boundary  in  Western  Pennsylvania,  Ohio,  Kentucky,  Indiana,  and  Illinois,  by  George 
Frederick  Wright,  with  an  introduction  by  Thomas  Chrowder  Chamberlin.  1890.  8°.  112  pp.  incl. 
1 pi.  8 pi.  Price  15  cents. 

59.  The  Gabbros  and  Associated  Rocks  in  Delaware,  by  Frederick  D.  Chester.  1890.  8°.  45  pp. 
1 pi.  Price  10  cents. 

60.  Report  of  work  done  in  the  Division  of  Chemistry  and  Physics,  mainly  during  the  fiscal  year 

1887- 88.  F.  W.  Clarke,  chief  chemist.  1890.  8°.  174  pp.  Price  15  cents. 

61.  Contributions  to  the  Mineralogy  of  the  Pacific  Coast,  by  William  Harlow  Melville  and  Waldemar 
Lindgren.  1890.  8°.  40  pp.  3 pi.  Price  5 cents. 

62.  The  Greenstone  Schist  Areas  of  the  Menominee  and  Marquette  Regions  of  Michigan  ; a contri- 
bution to  the  subject  of  dynamic  metamorphism  in  eruptive  rocks,  by  George  Huntington  Williams; 
with  an  introduction  by  Roland  Duer  Irving.  1890.  8°.  241  pp.  16  pi.  Price  30  cents. 

63.  A Bibliography  of  Paleozoic  Crustacea  from  1698  to  1889,  including  a list  of  North  American 
species  and  a systematic  arrangement  of  genera,  by  Anthony  W.  Vogdes.  1890.  8°.  177  pp.  Price 

15  cents. 

64.  A Report  of  work  done  in  the  Division  of  Chemistry  and  Physics,  mainly  during  the  fiscal  year 

1888- ’89.  F.  W.  Clarke,  chief  chemist.  1890.  8°.  60  pp.  Price  10  cents. 

66.  On  a Group  of  Volcanic  Rocks  from  the  Tewan  Mountains,  New  Mexico,  and  on  the  occurrence 
of  Primary  Quartz  in  certain  Basalts,  by  Joseph  Paxson  Iddings.  1890.  8°.  34  pp.  Price  5 cents. 

In  press: 

65.  Comparative  Stratigraphy  of  the  Bituminous  Coal  Rocks  of  the  Northern  Half  of  the  Appala- 
chian Field,  by  I.  C.  White. 

67.  The  relations  of  the  Traps  of  the  Newark  System  in  the  New  Jersey  Region,  by  N.  H.  Darton. 

68.  Earthquakes  in  California  in  1889,  by  J.  E.  Keeler. 

69.  A Classed  and  Annotated  Bibliography  of  Fossil  Insects,  by  Samuel  Hubbard  Scudder. 

In  preparation 

— The  Viscosity  of  Solids,  by  Carl  Barus. 

— Mesozoic  Fossils  in  the  Permian  of  Texas,  by  C.  A.  White. 

— A Late  Volcanic  Eruption  in  Northern  California  and  its  Peculiar  Lava,  by  J.  S.  Diller. 

— Altitudes  between  Lake  Superior  and  the  Rocky  Mountains,  by  Warren  Upham. 

— A Bibliography  of  Paleobotany,  by  David  White. 

STATISTICAL  PAPERS. 

Mineral  Resources  of  the  United  States,  1882,  by  Albert  Williams,  jr.  1883.  8°.  xvii,  813  pp.  Price 
50  cents. 

Mineral  Resources  of  the  United  States,  1883  and  1884,  by  Albert  Williams,  jr.  1885.  8°.  xiv,  1016 
pp.  Price  60  cents. 

Mineral  Resources  of  the  United  States,  1885.  Division  of  Mining  Statistics  and  Technology.  1886. 
8°.  vii,  576  pp.  Price  40  cents. 

Mineral  Resources  of  the  United  States,  1886,  by  David  T.  Day.  1887.  8°.  viii,  813  pp.  Price  50 
cents. 

Mineral  Resources  of  the  United  States,  1887,  by  David  T.  Day.  1888.  8°.  vii,  832  pp.  Price  50 
cents. 

Mineral  Resources  of  the  United  States,  1888,  by  David  T.  Day.  1890.  8°.  vii,  652  pp.  Price  50 
cents. 

The  money  received  from  the  sale  of  these  publications  is  deposited  in  the  Treasury,  and  the  Secre- 
tary of  the  Treasury  declines  to  receive  bank  checks,  drafts,  or  postage  stamps ; all  remittances,  there- 
fore, must  be  by  postal  note  or  money  order,  made  payable  to  the  Librarian  of  the  U.  S.  Geological 
Survey,  or  in  currency,  for  the  exact  amount.  Correspondence  relating  to  the  publications  of  the 
Survey  should  be  addressed 

To  the  Director  of  the 

United  States  Geological  Survey. 

Washington,  D.  C. 


Washington,  D.  C.,  September , 1890. 


DEPARTMENT  OP  THE  INTERIOR 


BULLETIN 

OF  THE 

UNITED  STATES 


GEOLOGICAL  SURVEY 


No.  62 


WASHINGTON 

GOVERNMENT  PRINTING  OFFICE 
1890 


UNITED  STATES  GEOLOGICAL  SURVEY 

J.  W.  POWELL,  DIRECTOR 


THE  GREENSTONE  SCHIST  AREAS 

OF  THE 


A CONTRIBUTION  TO  THE  SUBJECT  OF  DYNAMIC  METAMORPHISM 
IN  ERUPTIVE  ROCKS 


BY 

GEORGE  HUNTINGTON  WILLIAMS 


WITH  AN  INTRODUCTION  BY 


ROLAND  DUER  IRVING 


WASHINGTON 

GOVERNMENT  PRINTING  OFFICE 
1890 


CONTENTS. 


Page. 

Letter  of  transmittal,  by  R.  D.  Irving 9 

Explanatory  and  historical  note,  by  R.  D.  Irving 11 

Introduction 31 

Chapter  I.  Present  state  of  our  knowledge  regarding  the  metamorphism  of 

eruptive  rocks 34 

Value  of  the  microscope  in  the  study  of  metamorphism 34 

Historical  outline  of  studies  on  the  metamorphism  of  eruptive  rocks 40 

Chapter  II.  Greenstone  belts  of  the  Menominee  iron  district 64 

Introductory  and  historical 64 

Sturgeon  Falls 67 

Lower,  or  Little  Quinnesec  Falls 77 

Chapter  III.  Greenstone  belts  of  the  Menominee  iron  district  (continued). ..  96 

Upper,  or  Big  Quinnesec  Falls 96 

The  dark  colored  greenstones  of  the  basin 97 

The  light  colored  greenstones  at  Upper  Quinnesec  falls 102 

The  coarse  grained  diorites  of  the  Horse  Race 106 

The  acid  rocks  of  the  Upper  Quinnesec  Falls  and  Horse  Race 110 

Four- foot  Falls 123 

The  Twin  Falls 127 

Lower  Twin  Falls 129 

Upper  Twin  Falls. 132 

Chapter  IV.  Greenstone  belts  of  the  Marquette  district 134 

Introductory 134 

Rocks  of  the  northern  portion  of  the  Marquette  area 138 

Basic  intrusives 138 

Acidintrusives 146 

Banded  greenstone  schists 154 

Chapter  V.  Greenstone  belts  of  the  Marquette  district  (continued) 163 

Rocks  of  the  southern  portion  of  the  Marquette  area 163 

The  aphanitic  greenstones 163 

Coarse  grained  dike  rocks 168 

Greenstones  south  of  the  quartzite 170 

Rocks  of  the  Negauuee  area 171 

Aphanitic  greenstones 171 

Coarsely  crystalline  greenstones 173 

The  stretched  fragmental  rocks  on  the  Carp  River 175 

Acid  rocks 178 

Rocks  of  the  Northern  area. 179 

Unaltered  basic  intrusives 180 

Altered  coarse  grained  rocks 180 

Banded  greenstones 184 

Green  schists  and  agglomerates  of  Deer  Lake 185 

5 


6 


CONTENTS. 


Page. 

Chapter  VI. — General  results  and  conclusions 192 

Original  character  of  the  Menominee  and  Marquette  greenstone  areas 192 

Evidence  of  eruptive  character 192 

Different  original  rock  types 197 

Original  mineral  constituents 199 

Conditions  under  which  the  greenstones  were  formed 200 

Macrostructural  metamorphism  of  the  Menominee  and  Marquette  massive 

rocks 201 

Macrostructural  metamorphism  through  compression,  faulting,  or 

crushing 202 

Macrostructural  metamorphism  through  stretching 204 

Microstructural  metamorphism  of  the  Menominee  and  Marquette  massive 

rocks 204 

Effects  of  dynamic  action  on  individual  minerals 205 

New  structures  produced  by  dynamic  action 206 

Mineralogical  (chemical)  metamorphism  of  the  Menominee  and  Marquette 

massive  rocks 208 

Secondary  minerals  and  their  origin 209 

Progress  of  alteration  in  the  original  minerals 214 


ILLUSTRATIONS. 


Plate  I.  Outline  geological  map  of  the  Marquette  region 

II.  Outline  geological  map  of  the  Menominee  iron  region 

III.  Map  of  Sturgeon  Falls,  Menominee  River  (after  Brooks) 

IV.  Map  of  Lower  Quinnesec  Falls,  Menominee  River  (after  Brooks). 

V.  Map  of  Upper  Quinnesec  Falls,  Menominee  River  (after  Brooks) . 

VI.  Map  of  Twin  and  Four-toot  Falls,  Menominee  River  (after  Brooks) 

VII.  Map  of  the  environs  of  Marquette 


IX. 


XVI. 


Fig. 

1. 

2. 

Fig. 

1. 

2. 

Fig. 

1. 

2. 

Fig. 

1. 

2. 

Fig. 

1. 

2. 

Fig. 

1. 

2. 

Fig. 

1. 

2. 

Fig. 

1. 

2. 

Fig. 

1. 

Saussurite  gahbro  (first  stage) 

2.  Saussurite  gabbro  (second  stage) 

1.  Altered  diabase  or  diorite 

2.  Schistose  band  in  the  last  figured  rock,  showing  the  effect 

of  dynamic  metamorphism  (stretching)  upon  it 

1.  Saussurite  diorite 

2.  Typical  aphanitic  greenstone  of  the  Marquette  region.. 

1.  Chlorite-epidote  aggregate  in  an  altered  diabase 

2.  Stretched  greenstone 

1.  Coarsely  crystalline  diorite 

2.  Epidiorite  

1.  Sphene  crystals  around  ilmenite 

Rutile  originating  from  the  alteration  of  ilmenite 

1.  Sericite  porphyry 

Stretched  and  brecciated  greenstone 

1.  Structure  of  one  of  the  u eyes”  in  an  “Augengneiss  ” or 

stretched  granite  porphyry 

2.  Stretched  quartz  porphyry 

1.  Greenstone  schists  (tuffs)  of  the  northern  Marquette  area 

Ampliibole  granite  (?)  forming  a dike  in  the  aphanitic 
greenstones 


Page. 

14 

24 

68 

86 

96 

124 

138 

222 

222 

224 

224 

226 

226 

228 

228 

230 

230 

232 

232 

234 

234 

236 

236 

238 

238 


Fig.  1.  Hypothetical  section  of  the  Menominee  region  in  the  vicinity  of 


Quinnesec  (after  Brooks) 26 

2.  Hypothetical  section  of  the  Menominee  region  in  the  vicinity  of  Twin 

Falls  (after  Brooks) 27 

3.  Hypothetical  section  of  the  Menominee  region  in  the  vicinity  of  Quin- 

nesec (by  R.  D.  Irving) 30 

4.  Twinning  lamellie  in  secondary  albite 69 

5.  Zoisite  crystals  in  saussurite 69 

6.  Zoisite  crystal  showing  position  of  optical  constants  with  reference  to 

cleavage  lines 70 

7.  Compact  and  fibrous  secondary  hornblende 70 

8.  Helminth  (vermicular  chlorite)  in  quartz 71 

9.  Hornblende  altering  to  chlorite 79 

10.  Cross  gashes  in  greenstone  produced  by  stretching 81 

11.  Broken  feldspar  crystals  in  crushed  and  stretched  greenstone 105 


7 


8 


ILLUSTRATIONS. 


Page. 


Fig.  12.  Rutile  needles  (Thonschiefernadeln) 106 

13.  Broken  tourmaline  crystal  proving  the  secondary  fracture  of  the  in- 

closing quartz 112 

14.  Foliated  granite  (gneiss)  intrusive  in  greenstone 115 

15.  Foliated  granite  (gneiss)  intrusive  in  greenstone 115 

16.  Foliated  granite  (gneiss)  intrusive  in  greenstone 116 

17.  Orthite  (allanite)  in  granite 117 

18.  Broken  zircon  crystal  in  schistose  porphyry 122 

19.  Compact  surrounded  by  fibrous  hornblende  (secondary  growth?)  126 

20.  Rhomboidal  parting  in  greenstone  (diagrammatic) 128 

21.  Acute  rhomboidal  parting  in  greenstone  (diagrammatic) 128 

22.  Schistose  parting  developed  from  that  in  Fig.  21 128 

23.  Greenstone  made  schistose  by  faulting 129 

24.  Greenstone  made  schistose  by  faulting 130 

25.  Anatase  formed  by  the  alteration  of  ilmenite  in  greenstone 131 

26.  Spheroidal  parting  of  aphanitic  greenstone  produced  by  brecciation..  166 

27.  Same  as  in  Fig.  26,  drawn  out  into  lenses  by  pressure 177 

28.  Bent  hornblende  crystal 183 

29.  Surface  of  agglomerate  from  Deer  Lake 188 


LETTER  OF  TRANSMITTAL. 


United  States  Geological  Survey, 

Lake  Superior  Division, 
Madison , Wisconsin , February  10,  1888. 

Sir  : I have  the  honor  to  transmit  herewith,  for  publication  as  a 
bulletin  of  the  Survey,  a paper,  by  Prof.  George  H.  Williams,  of  Balti- 
more, Maryland,  on  The  Greenstone-Schist  Areas  of  the  Marquette  and 
Menominee  Regions  of  Michigan. 

The  exact  object  and  bearing  of  the  work  thus  accomplished  by 
Prof.  Williams  I have  set  forth  in  an  explanatory  and  historical  note 
prefixed  to  his  memoir. 

I am,  sir,  very  respectfully,  yours, 

R.  D.  Irving, 

Geologist  in  Charge . 

Hon.  J.  W.  Powell, 

Director  U.  S.  Geological  Survey. 


9 


EXPLANATORY  AND  HISTORICAL  NOTE. 


By  Roland  Duer  Irvino. 


At  quite  a number  of  points  in  the  Lake  Superior  region  occu*  pecu- 
liar schistose  rocks,  which  combine  with  a prevalent  fi  ne  grain  a general 
tendency  to  greenish  color.  Besides  occurring  here  and  there  more  or 
less  confusedly  mingled  with  masses  of  granite  and  other  rocks,  these 
greenish  schists  occur  also  in  large  continuous  areas,  which  they  entirely 
occupy,  except  for  certain  relatively  unimportant  basic  and  acid  intru- 
sives.  Microscopic  study  has  shown  that  these  rocks  are  at  times  fully 
developed  hornblende  schists,  and  again  glossy  kinds,  in  which  chlorite 
is  so  important  an  ingredient  as  to  warrant  our  calling  them  chlorite 
schists.  In  other  places  again  they  are  more  massive,  and  present  more 
or  less  distinctly  the  appearance  of  fine-grained  basic  eruptives;  but 
the  bulk  of  these  areas  is  composed  of  nondescript  fine-grained  green- 
ish schists,  which  appear  to  grade  into  the  more  massive  greenstone-like 
forms  on  the  one  hand,  and  into  the  more  distinctly  developed  chloritic 
and  hornblendic  schists  on  the  other.  As  a rule  these  various  schists 
present  no  parallel  structure  other  than  that  which  seems  referable 
directly  to  secondary  causes ; that  is  to  say,  they  do  not  present  such 
banded  varieties  as  would  suggest  the  action  of  sedimentation  during 
their  production.  However,  such  banded  varieties  do  occur  in  subordi- 
nate quantity,  presenting  then  very  strikingly  regular,  rapid  alterna- 
tions of  light  and  dark  bands. 

Again,  here  and  there  in  these  peculiar  areas,  in  some  places  with  a 
very  considerable  development,  there  occur  kinds  which  present  a more 
or  less  obscure  fragmental  appearance,  this  appearance  being  generally 
far  more  pronounced  on  a weathered  surface  than  on  a fresh  one,  on 
which  latter  the  matrix  and  the  parent  fragments  are  apt  to  look  much 
like  one  another,  either  from  original  similarity  in  character  or  from 
having  undergone  alterations  which  have  led  both  fragments  and 
matrix,  originally  different,  to  similar  results.  At  times  there  is  a co- 
incidence of  occurrence  between  the  banding  above  referred  to  and  the 
appearance  of  the  pebble-bearing  forms,  but  so  far  as  my  experience 
goes  this  is  very  commonly  not  the  case,  the  fragmental  phases  being 
without  any  parallel  structure  other  than  the  general  secondary  cleav- 
age, which  all  of  these  rocks  present,  the  apparent  pebbles  occurring 
more  commonly  in  tumultuous  assemblages  of  masses  of  all  sizes. 


12 


GREENSTONE  SCHIST  AREAS  OF  MICHIGAN. 


[BULL.  62. 


As  prominent  illustrations  of  such  green  schist  areas,  there  may  be 
mentioned  that  which  runs  directly  westward  from  the  shore  of  Lake 
Superior  at  Marquette,  Michigan,  for  a distance  ofj  some  twenty  miles, 
with  a width  ranging  from  two  to  six  miles ; 1 those  which  occur  in  the 
Menominee  Yalley,  on  the  boundary  between  Wisconsin  and  Michigan;2 
that  of  the  Gogebic  country  of  western  Michigan,  in  T.  47  NT.,  E.  43  W., 
and  T.  47  N.,  E.  44  W.,  where  there  is  a very  great  development  of  the 
fragmental  phases;3  that  which  has  been  recently  outlined  by  Dr.  W. 

S.  Bayley  to  the  south  of  the  so-called  Mesabe  Eange,  and  west  of 
the  Embarras  Lakes,  in  T.  59  N.,  E.  15  W.,  and  T.  59  N.,  E.  16  W., 
northern  Minnesota,  where  there  is  again  a considerable  development 
of  the  fragmental  forms ; 4 and  that  which  lies  to  the  northward  of  the 
iron-bearing  slates  of  Yermillion  Lake,  traversing  the  island  in  the 
northern  part  of  that  Jake  from  west  to  east,  and  extending  thence  east 
and  northeast,  with  an  average  width  of  from  two  to  three  miles,  through 
townships  62,  63,  64,  and  65  N.,  of  ranges  14,  13, 12, 11,  10,  and  9 W.,  in 
northern  Minnesota,  to  the  national  boundary  line  at  Carp  Lake,  whence 
it  extends  an  unknown  distance  into  Canada.  This  last-named  area, 
which  is  the  most  extended  continuous  one  with  which  I am  acquainted, 
shows  prevalently  those  kinds  of  rock  which  lack  the  fragmental  ap- 
pearance. Still,  fragmental  phases  here  and  there  present  themselves, 
as,  for  instance,  along  the  east  shore  of  that  island  in  Yermillion  Lake, 
which  lies  in  the  northern  part  of  Sec.  10  and  southern  part  of  Sec.  3, 

T.  62  N.,  E.  16  W.  To  these  areas  may  be  added  also  several  smaller 
ones  which  lie  southward  and  southeastward  of  the  Yermillion  Lake  iron 
belt.  One  of  these  areas,  lying  south  of  Sea  Gull  Lake  and  east  of 
Ogishkimanissi  Lake,  in  T.  65  N.,  E.  5 W.,  presents  an  extraordinary 
development  of  the  obscurely  fragmental  or  brecciated  phase.  Finally, 
should  be  mentioned  the  large  development  of  similar  greenish  schists, 
including  also  the  fragmental  or  “ agglomeratic  ” phases,  which  is 
described  as  occurring  on  the  Lake  of  the  Woods  in  the  recent  report 
of  Mr.  A.  C.  Lawson,  of  the  Canadian  Survey.5 

My  first  acquaintance  with  any  of  these  green  schist  areas  was  in  the 
summer  of  1883,  when  a number  of  days  were  spent  in  examining  the 
exposures  at  Twin  Falls,  Upper  Quinnesec  Falls  and  Lower  Quinnesec 
Falls,  on  the  Menominee  Eiver,  the  boundary  between  Wisconsin  and 
Michigan.  The  very  handsome  detailed  maps  and  the  descriptions  of 
these  exposures  by  Maj.  T.  B.  Brooks6  had  already  been  published  and 

1 See  map  of  T.  B.  Brooks,  Geol.  Survey  Michigan,  Atlas,  PI.  Ill  $ map  by  C.  Kominger,  accompany- 
ing Geol.  Survey  Michigan,  Vol.  4,  1881 ; PI.  I of  the  present  volume. 

2 See  map  by  T.  B.  Brooks  and  C.  E.  Wright,  PI.  28  of  the  atlas  to  the  Geology  of  Wisconsin  ; map 
by  C.  E.  Wright,  PI.  30  of  the  same  atlas ; map  of  the  Menominee  region,  by  C.  Rominger,  Geol.  Sur- 
vey Michigan,  Vol.  4,  1881,  PI.  2. 

3 See  maps  by  It.  D.  Irving  and  C.  It.  Van  Hise,  accompanying  a memoir  on  the  Penokee-Gogebio 
iron  region,  Mon.  U.  S.  Geol.  Survey,  No.  18. 

4 See  map  by  It.  D.  Irving,  PI.  XLI,  of  the  Seventh  Ann.  Kept.  U.  S.  Geol.  Survey. 

6See  Geol.  Nat.  Hist.  Survey  Canada,  Ann.  Rep.  (new  series)  Vol.  1,  1885,  pp.  41-46  cc;  also  map 
accompanying  same. 

6Ge[>l.  Wisconsin,  vol.  3,  1880. 


iBvufG.  1 EARLY  IMPRESSIONS  OF  MENOMINEE  GREENSTONES.  id 

were  used  on  the  ground.  These  maps  represent  the  exposures  at  the 
several  points  named  as  composed  of  a series  of  very  regular  alterna- 
tions of  various  schistose  and  massive  rocks,  the  conclusion  being 
reached  with  regard  to  them  by  Brooks  that  they  form  in  all  a regular 
series  of  layers  originally  of  sedimentary  origin,  the  present  lack  of  frag- 
mental appearance  being  taken  as  the  result  of  metamorphism.  To  me 
it  seemed  at  that  time  that  the  regularity  of  the  alternations  was  far 
less  than  one  would  think  to  be  the  case  from  Brooks’s  maps,  and  that  all 
of  the  several  phases,  schistose  and  non- schistose,  were  rather  vari- 
ations of  one  great  mass  of  material,  whose  original  structure  was  mass- 
ive rather  than  schistose.  This  impression  was  gathered  from  the  way 
in  which  the  several  phases  graded  into  one  another,  and  from  the  non- 
continuity in  the  direction  of  the  strike  of  the  schistose  kinds,  single 
schist  beds  displayed  on  one  side  of  the  stream  being  often  absent 
where  their  continuations  should  lie  on  the  opposite  side  of  the  stream. 
The  impression  was  strengthened  by  the  lack  of  regularity  in  the  di- 
rection of  the  schist  planes,  and  by  the  striking  way  in  which  schist 
bands  inclose  vaguely  outlined  areas  of  non-schistose  massive  rocks. 
The  same  conclusion  as  to  the  inseparable  nature  of  all  of  these  rocks 
had  already  been  reached  and  published  by  Rominger,1  though  he  ap- 
pears to  have  looked  upon  the  parallel  or  schistose  structure  as  repre- 
senting an  original  condition  of  the  rocks,  all  of  which  he  seems  to 
consider  of  sedimentary  origin;  while  the  impression  made  on  me  was 
iust  the  opposite,  namely,  that  the  schistosity  is  of  a secondary  nature, 
and  the  original  structure  of  the  rock  a massive  one.  In  order  to  test 
this  question,  a large  collection  of  specimens,  with  quite  full  notes,  was 
made  at  the  time.  In  the  next  year,  however,  before  the  thin  sections 
made  from  these  specimens  could  be  examined,  the  entire  collection 
was  destroyed  by  fire,  and  my  work  in  other  directions  having 
become  pressing,  it  was  decided  to  put  the  study  of  this  question  in 
the  hands  of  Prof.  George  H.  Williams,  of  the  John  Hopkins  Uni- 
versity, whose  qualifications  for  investigations  in  microscopic  petrog- 
graphy,  such  as  this  would  mainly  be,  are  well  known  to  be  of  the  first 
order.  In  the  summer  of  1885,  therefore,  Professor  Williams  made,  at 
my  request,  a reexamination  of  all  of  these  points  in  the  Menominee 
valley,  going  into  far  greater  detail  in  the  field  study  than  any  one 
had  done  before,  and  collecting  on  a very  large  scale.  During  the 
summer  of  1886,  Professor  Williams  was  asked  to  extend  his  field  ex- 
aminations into  the  Marquette  greenschist  area,  and  here  similar  de- 
tailed studies  and  large  collections  were  made.  The  present  publica- 
tion is  the  result  of  Professor  Williams’s  work,  which  has  included  the 
detailed  examination  of  about  400  thin  sections  made  from  the  speci- 
mens gathered. 

While  Professor  Williams’s  investigations  have  been  going  on,  the 
various  other  green  schist  areas  named,  so  far  as  they  lie  within  the 


Geol.  Survey  Michigan,  vol.  4,  1881,  p.  214. 


14  GREENSTONE  SCHIST  AREAS  OF  MICHIGAN.  [bull.  62. 

boundary  of  the  United  States,  have  been  examined  in  considerable  de- 
tail, large  collections  and  extensive  field-notes  having  been  gathered  by 
Prof.  Yan  Hise,  Messrs.  W.  N.  Merriam  and  W.  S.  Bay  ley,  and  myself. 
These  additional  collections  are  now  quite  thoroughly  sectioned,  and  it 
is  hoped  soon  to  study  them  in  detail,  and  to  offer  a second  contribution 
to  our  knowledge  of  this  important  class  of  rocks.  The  present  publi- 
cation, however,  deals  only  with  the  Marquette  and  Menominee  areas. 

Prof.  Williams’s  investigations  having  been  directed  especially  to  a 
microscopic  study  of  these  peculiar  greens  chists,  with  the  object  of  ascer- 
taining whether  such  study  would  throw  any  light  upon  their  original 
condition ; it  does  not  come  within  the  province  of  his  memoir  to  discuss 
the  geologic  relations  of  the  green  schist  masses  as  wholes.  Neverthe- 
less, it  is  almost  unavoidable  that  some  reference  should  be  made  in  this 
volume  to  these  geological  relations,  and,  since  there  has  been  a good 
deal  of  difference  of  opinion  as  to  them  among  the  several  geologists 
who  have  written  upon  the  Menominee  and  Marquette  areas,  it  seems 
necessary  to  explain  briefly  the  different  views  that  have  been  advanced, 
including  the  conclusions  to  which  my  own  studies  have  thus  far  led  me, 
though  without  attempting  any  general  discussion  of  the  subject  for 
the  whole  Lake  Superior  region.  Such  a discussion  it  is  designed  to  leave 
until  exhaustive  microscopic  studies,  like  that  of  Professor  Williams  here 
presented,  shall  have  been  extended  over  the  other  areas  of  similar  rocks 
above  named.  We  shall  then  be  in  possession  not  only  of  all  available 
structural  facts  with  regard  to  these  peculiar  rocks,  but  also  of  all  that 
the  most  refined  methods  of  study  can  give  us  with  regard  to  their  in- 
ternal texture  and  mineralogical  composition. 

The  map  (PI.  I)  shows,  in  a general  way,  the  distribution  of  the  dif- 
ferent kinds  of  rocks  in  the  vicinity  of  Marquette.  In  preparing  this 
map,  those  by  Brooks  and  Bominger,  read  in  the  light  of  my  own  studies 
in  this  region,  have  been  used.  It  should  be  said  that  a detailed  map 
of  the  Marquette  district  has  not  been  attempted  by  the  U.  S.  Geologi- 
cal Survey  as  yet,  partly  because  other  more  pressing  work  was  in  prog- 
ress, and  partly  because  without  a thoroughly  accurate  topographical 
basis  for  such  a map  it  has  not  been  thought  that  much  advance  could 
be  made  upon  the  several  maps  heretofore  constructed.  It  is  proposed, 
however,  to  begin  such  topographical  survey  immediately,  and  upon 
the  basis  thus  prepared,  to  place  everything  exactly  as  it  is  seen,  and, 
making  use  of  all  the  latest  mining  developments,  to  attempt  to  work 
out  accurately  and  in  detail  the  structure  of  the  region  in  such  a fash- 
ion that  what  is  inferred  may  be  easily  separated  from  what  is  actually 
known. 

Upon  the  present  map  the  large  area  colored  for  greenstone  schists 
is  the  one  which  came  particularly  under  Professor  Williams’s  investiga- 
tions. Northward  this  area  is  limited,  in  the  eastern  portion,  by  a great 
spread  of  granitic  and  gneissic  rocks.  The  line  of  demarkation  between 
the  schists  and  the  granites,  however,  is  not  a sharp  one,  since  the 


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ARCH  EAN. 


AGE  L 


Granite  and  Gneiss.  Greenstone  Schists.  Altered 


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OUTLINE  GEOLOGICAL  MAI 

Compiled  by  R.D.Irviiuj  ir omnia 


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BULLETIN  No. 62  PLATE  I. 


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Iron  Bearing  Serie  s . Lake  Superior  S.  S . 
< Detritals,  Limestones  and 
Femujinous  Schists, with interbedded 
Greenstones.) 


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DF  THE  MARQUETTE  REGION. 

by  T.B.Rrooks  and  (’.Romincjer. 
miles. 


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til 


IBV1NG.1 


GREENSTONE  SCHISTS  NEAR  MARQUETTE. 


15 


two  seem  to  mingle  more  "or  less  confusedly  on  each  side  of  the  some- 
what arbitrary  line  indicated  upon  the  map.  Southward  of  this  green- 
stone-schist area,  and  again  dovetailing  into  it  on  the  north,  are  belts 
of  country  occupied  mainly  by  detrital  rocks,  such  as  quartzites  and 
various  fragmental  slates;  with  these,  however,  are  large  bodies  of 
crystalline  limestone  and  several  phases  of  ferruginous  schist,  all 
of  which  have  in  common  an  entire  lack  of  anything  like  a frag- 
mental texture.  In  addition  to  these  rocks  these  areas  include  also 
sheets  of  diabasic  greenstone,  which  are  interbedded  with  the  detritals 
and  ferruginous  schists  alluded  to.  On  the  south  of  the  southernmost 
of  these  detrital  areas,  in  which  are  included  all  the  well  known  iron 
mines  of  the  Marquette  region,  is  again  a large  area  of  granitic  and 
gneissic  rocks. 

The  greenstone  schists  are  affected  generally  by  a vertical  or  nearly 
vertical  cleavage  structure,  to  which  the  occasional  banding  of  the 
rock,  suggestive  of  a sedimentary  origin,  is  also  parallel.  The  layers 
of  rock  of  which  the  detrital  areas  are  composed  are  affected  partly  by 
a similar  cleavage  structure,  but,  on  the  whole,  far  less  markedly  so, 
while  the  bedding  of  these  rocks  is  as  a rule  very  distinct,  and  indi- 
cates a more  or  less  open  or  gentle  bowing  of  the  layers,  the  dips  being 
at  times  southward  and  again  northward,  and  usually  at  a much  lower 
angle  than  is  the  cleavage  structure  of  the  greenstone  schists.  At 
times,  however,  particularly  in  the  easternmost  portion  of  the  southern 
of  these  two  belts,  the  inclinations  of  the  detrital  rocks  are  much  higher, 
and  then  bedding  and  cleavage  structure  approach  to  parallelism  with 
each  other,  and  with  the  cleavage  structure  of  the  greenstone  schists 
further  north.  While  folded  back  and  forth,  these  detrital  areas  show 
for  the  most  part  an  evident  general  synclinal  structure;  that  is  to  say, 
the  layers  of  rock  of  which  they  are  composed,  as  they  appear  along  the 
edges  of  these  areas,  dip  inward  towards  their  middle  portions.  Thus 
the  greenstone  schists  seem  plainly  to  rise  from  beneath  the  higher  de- 
trital layers.  As  to  the  inferior  position  of  these  greenstone  schists  to 
the  detrital  iron-bearing  rocks,  all  geologists  who  have  examined  this 
region  would  probably  agree;  at  all  events  all  those  who  have  expressed 
themselves  with  regard  to  the  matter  seem  to  have  no  hesitation  con- 
cerning it. 

Foster  and  Whitney,  whose  classical  work1  gives  the  first  compre- 
hensive account  of  the  geology  of  this  region,  do  not  appear  to  have 
separated  the  greenstone  schists  from  the  other  stratiform  rocks  in  such 
a fashion  as  to  indicate  their  exact  strati  graphical  relations.  All  of 
these  stratiform  rocks  they  appear  to  have  looked  upon  as  constituting 
one  great  series,  whose  crumpled  condition  they  attributed  to  the  sub- 
sequent eruption  of  the  granite  masses  on  either  side  of  the  single 
trough,  which  they  regarded  the  stratiform  rocks  as  occupying.2  They 


•Report  of  the  geology  of  the  Lake  Superior  land  district,  by  J.  W.  Foster  and  J.  D.  Whitney,  pt.  2. 
The  Iron  Region,  Washington,  1851. 

’Ibid.,  p.  41,  Fig.  5. 


16 


GREENSTONE  SCHIST  AREAS  OF  MICHIGAN. 


[BULL.  62. 


appear,  however,  to  refer  especially  to  the  greenstone  schists  in  the 
following: 

Many  of  the  slates  appear  to  be  composed  of  pulverulent  greenstone,  as  though  they 
might  originally  have  been  ejected  as  an  ash,  and  subsequently  deposited  as  a sedi- 
ment, and  pass  by  imperceptible  gradations,  from  a highly  fissile  to  a highly  compact 
state.  * * * The  slates  are  composed  essentially  of  the  same  ingredients  as  the 
trappean  rocks  with  which  they  are  associated,  and  the  main  difference  between 
them  may  be  that  the  one  was  the  product  of  salses,  ejected  in  the  form  of  mud,  while 
the  other  was  the  product  of  volcanoes,  ejected  in  molten  streams.1 

They  appear  also  to  refer  especially  to  the  greenstone  schists  when 
they  speak  of  the  stratiform  series  as  exhibiting  greater  alteration  in 
the  vicinity  of  the  masses  of  eruptive  granite,  than  at  distances  from 
these  masses.2 

J.  P.  Kimball,  who  wrote  in  1864, 3 considered  the  granitic  and  gneissic 
masses  on  either  side  of  the  belt  of  stratiform  rocks,  as  correspond- 
ing to  the  Laurentian  series  of  Canada,  while  he  parallelized  the  whole 
of  the  stratiform  succession  with  the  Huronian  series  of  the  north  shore 
of  Lake  Huron,  thus  making  the  granitic  and  gneissic  rocks  the  older 
basement  upon  which  all  of  the  stratiform  Huronian  was  subsequently 
spread,  wholly  by  aqueous  agencies.  None  of  the  various  rocks  which 
Foster  and  Whitney  looked  upon  as  eruptive,  are  thought  by  Kimball 
to  have  had  that  origin,  even  the  various  greenstones  being  taken  to  be 
metamorphic  sedimentary  material.  In  the  case  below  Kimball  appears 
to  refer  particularly  to  the  greenstone  schists,  which  form  our  present 
subject,  and  which,  it  thus  appears,  he  looked  upon  as  the  basement 
member  of  the  Huronian  succession.  He  says:4 

The  gneiss  which  marks  the  boundary  of  the  granite  belts,  and  accordingly  char- 
acterizes the  top  of  the  Laurentian  series  in  this  region,  the  same  as  it  is  elsewhere 
represented,  is  succeeded  by  dark  colored  hornblendic  schists,  which  consequently 
represent  the  base  of  the  Azoic  or  Huronian  series.  These  schists  are  followed  by  a 
series  of  augitic  rocks  and  schists,  interstratified  with  magnesian  hydrous  rocks  and 
slates,  the  two  kinds  of  rocks  being  represented  on  the  one  hand  by  hypersthene,  pyr- 
oxene, and  bedded  diorite  passing  into  dioritic  slates,  and  on  the  other  by  talcose 
and  chloritic  schists.  The  former  character  of  rocks  prevails  to  such  an  extent  as  to 
impart  to  the  lower  members  of  the  Huronian  series  a distinctive  augitic  aspect. 
The  several  rocks  composing  this  augitic  zone  are  commonly  of  a greenish  color,  and 
vary  in  this  respect  chiefly  as  to  shade,  resembling  in  this  particular  the  Lower  Slate 
Conglomerate,  which  marks  the  base  of  the  series  in  Canada,  and  from  which  they 
seem  to  differ  only  in  the  absence  of  pebbles  and  bowlders  from  the  subjacent  Lau- 
rentian rocks,  which  there  form  a distinguishing  feature.5  * 

1 Report  of  the  geology  of  the  Lake  Superior  land  district,  by  J.  W.  Foster  and  J.  D.  Whitney,  pt.  2. 
The  Iron  Region,  Washington,  1851,  pp.  16, 17. 

2 Ibid.,  p.  14. 

3 Am.  Jour.  Sci.,  2d  series,  vol.  39,  1865,  pp.  290-303. 

4 Ibid.,  p.  294. 

6 This  supposed  similarity  of  the  greenstone  schists  of  Marquette  to  the  Lower  Slate  Conglomerate 
of  Lake  Huron  is  not  borne  out  at  all  by  later  microscopic  and  field  studies.  Indeed,  the  two  have 
nothing  whatever  in  common,  unless  the  occasional  greenish  color  of  the  Lake  Huron  rocks  be  taken  to 
indicate  such  a resemblance.  The  Lower  Slate  Conglomerate  of  Lake  Huron,  with  its  granitic  and 
gneissic  pebbles,  proves  to  be  a mostcompletely  detrital  and  plainly  water- formed  mass  composed  chiefly 
of  fragments  of  quartz  and  feldspar,  with  the  alteration  products  of  the  latter,  the  whole  cemented  by 
a silicious  paste.  This  statement  is  made  only  after  a careful  examination  of  the  Labe  Huron  region, 
and  after  the  study  of  a ver}-  large  number  of  thiu  sections  from  Logan's  so-called  Lower  Slate  Con- 
glomerate. 


IRVING.] 


MARQUETTE  GREENSTONES. 


17 


T.  B.  Brooks,  upon  his  detailed  map  of  the  Marquette  district1  leaves 
blank  the  larger  part  of  the  area  occupied  by  the  greenstone  schists 
which  now  especially  concern  us,  indicating  here  and  there  upon  it, 
however,  the  occurrence  of  belts  of  “diorite”  and  of  “chloritic  and 
dioritic  schists.1’  All  of  these  rocks  he  evidently  regards  as  belonging 
conformably  beneath  the  detrital  quartzites  and  slates  which  form  his 
division  No.  V,  of  the  iron-bearing  series,  which  division  appears  in  a 
bold  ridge  along  the  northern  edge  of  the  southern  of  the  two  detrital 
areas  indicated  on  the  outline  map  herewith.  The  diorites  Brooks 
classes  lithologically  with  the  greenstones  interstratified  with  the  de- 
trital rocks  themselves,  though  apparently  looking  upon  them  as  be- 
longing to  much  lower  layers  in  the  succession.  In  this  lithological 
correlation,  as  will  be  seen  in  the  sequel,  Brooks  was  largely  correct, 
since  the  diorites  of  the  greenstone  schist  area  prove  to  be  diabasic 
greenstones  in  dike  form,  and  to  be  entirely  similar  lithologically  to  the 
interbedded  greenstones  of  the  detrital  or  iron-bearing  areas,  with  which 
they  are  also  presumably  wholly ‘contemporaneous.  All  of  these  rocks, 
both  massive  and  schistose,  Brooks  plainly  regarded  as  metamorphosed 
water-formed  sediments. 

Wadsworth,  writing  in  1880, 2 advocates  in  the  main  the  views 
presented  by  Foster  and  Whitney,  as  will  be  seen  by  the  following 
quotation : 

The  general  structure  of  the  country  would  seem  to  be  as  follows : The  schists, 
sandstones,  etc.,  having  been  laid  down  in  the  usual  way,  were  then  disturbed  by  the 
eruption  of  the  jasper  and  ore ; this  formed  the  knobs  of  jasper,  the  bauding  belong- 
ing to  the  fluidal  structure,  and  not  to  sedimentation.  Besides  occurring  in  bosses, 
the  jasper  was  spread  out  in  sheets,  and  intruded  through  the  rock  in  wedge-shaped 
masses,  sheets,  and  dikes.  Much  of  the  original  rock  still  remained  horizontal,  and 
new  sedimentary  deposits  continued  to  be  formed  out  of  the  jasper  and  the  other  rocks. 
Next  came  the  eruption  of  “ diorite,”  which  completed  most  of  the  local  folding  and 
tilting  of  the  strata.  Finally,  the  granite  eruption  took  place  on  both  sides  of  the 
“ Huronian,”  uplifting  and  contorting  the  strata  near  it,  and  perhaps  laterally  com- 
pressing the  inclosed  iron-bearing  rocks. 3 

Dr.  Wadsworth  does  not  appear  to  express  any  particular  opinion  as 
to  the  strati  graphical  position  of  the  greenstone  schists  of  the  area  now 
especially  under  consideration,  speaking  of  them  only  in  connection 
with  all  the  rest  of  the  stratiform  rocks  of  the  region  as  older  than  the 
adjacent  granite  areas.  The  greater  part  of  these  greenstone  schists 
he  would  seem  to  have  looked  upon  as  certainly  sedimentary,4  since  he 
records  a number  of  observations  going  to  show  that  there  is  no  grada- 
tion between  them  and  certain  dike-like  masses  occurring  with  them, 
using  these  observations  in  opposition  to  the  ideas  expressed  by  some 
of  his  predecessors  to  the  effect  that  inasmuch  as  the  massive  rocks  and 

'Geol.  Survey,  Michigan,  1873,  vol.  1,  Atlas  pi.  3.  See  also  pp.  99-104,  same  vol. 

3 Notes  on  the  Geology  of  tho  Iron  and  Copper  Districts  of  Lake  Superior.  By  M.  E.  Wadsworth 
Bull.  Mus.  Comp.  Zool.  Harvard  College,  Wholo  Scries,  vol.  7 (Geol.  Series,  vol.  1 No.  1). 

9 Ibid.,  p.  75.  4 Ibid.,  p.  37. 

Bull.  62 § 


18  GREENSTONE  SCHIST  AREAS  OF  MICHIGAN.  Ibull.  62. 

the  schists  grade  into  one  another,  the  former  are  of  sedimentary  origin 
as  well  as  the  latter.  That  there  are  genuine  dikes  intersecting  these 
schists  and  having  no  gradations  into  them,  Professor  Williams’s  observa- 
tions recorded  in  this  volume,  as  well  as  those  by  Rominger  and  others, 
make  very  plain,  although  even  in  the  case  of  these  genuine  later  dikes 
there  are  at  times  partially  schistose  forms  produced  apparently  by 
secondary  dynamic  agencies.  On  the  other  hand,  it  will  be  seen  from  Pro- 
fessor Williams’s  descriptions  that  there  are  other  massive  forms  among 
these  greenstone  schists  which  do  present  every  possible  gradation  into 
the  schists  themselves,  and  must,  therefore,  be  believed  to  have  had  a 
common  origin  with  them. 

Rominger,  in  his  account  of  the  geology  of  the  Marquette  region, 
published  in  1881, 1 describes  very  fully  the  greenstone-schist  area  which 
Professor  Williams  has  studied.  Rominger’s  mapping  of  this  area  has 
essentially  been  followed  upon  the  small  sketch-map  accompanying  the 
present  volume.  The  rocks  of  this  area  lie  describes  under  the  gen- 
eral head  of  the  u dioritic  group,”  which  group  he  looks  upon  as  form- 
ing the  basement  member  of  the  Huronian  series  within  which  he  would 
include  all  the  stratiform  rocks  of  the  region,  considering  it  as  placed 
conformably  beneath  the  detrital  strata.  The  origin  of  the  structure 
of  these  greenstone  schists  he  looks  upon  as  having  been  a secondary 
one,  although  he  recognizes  distinctly  their  intrusion  by  later  genuinely 
eruptive  dikes.  Inasmuch  as  in  its  more  northern  portion  the  green- 
stone-schist  area  presents  numerous  bosses  and  veins  of  gTanite,  he 
considers  these  as  proving  the  more  recent  origin  of  the  great  granite 
masses  lying  both  to  the  north  and  south  of  all  stratiform  rocks,  thus 
returning,  as  did  Wadsworth  before  him,  to  the  early  expressed  view 
of  Foster  and  Whitney,  with  whom  he  agrees  also  in  considering  that 
the  crumpling  of  all  of  the  stratiform  rocks,  greenstone  schists  and  de- 
tritals  as  well,  has  been  accomplished  by  the  protrusion  of  the  later 
granite  masses  on  either  side.  In  the  same  volume,  and  upon  his  map, 
Dr.  Rominger  indicates  numerous  small  areas  of  massive  and  schistose 
greenstones  as  occurring  in  the  vicinity  of  Negaunee  and  Ishpeming, 
within  the  district  represented  on  the  outline  map  herewith,  as  occupied 
entirely  by  the  detrital  iron-bearing  series.  These  masses  he  regards 
as  forming  portions  of  his  dioritic  group,  although  at  the  same  time 
recognizing  distinctly  the  fact  that  they  occur  at  various  horizons 
among  the  detritals,  which  he  looks  upon  as  lying  wholly  above  the 
main  mass  of  his  dioritic  rocks.  This  anomalous  arrangement  he  ex- 
plains by  representing  that  the  dioritic  group,  inasmuch  as  it  lies  at 
the  base  of  the  entire  stratiform  series,  comes  directly  into  contact 
with  the  granite  protrusions,  whose  metamorphosing  influence  was  so 
great  as  to  cause  the  fusion  of  a portion  of  these  basement  layers. 
These  fused  portions,  then,  he  imagines  to  have  intruded  themselves 
in  various  shapes  among  the  higher  detrital  layers.2  This  view,  how- 


1 Geol.  Survey  Michigan,  1881,  vol.  4,  with  map  of  Marquette  region, 

2 Ibid.,  pp.  22-39,  particularly  pp.  37,  38. 


IRVING.] 


MARQUETTE  GREENSTONES. 


19 


ever,  Dr.  Rominger  subsequently  abandoned,  as  will  appear  from  the 
following  quotation  from  the  manuscript  of  his  last  and  yet  unpub- 
lished report  :l 

As  from  the  massive  form  of  the  diorites  a gradation  exists  into  the  schistose  con- 
dition, and  as  schistose  structure  formerly  appeared  to  me  a positive  proof  of  a 
former  sedimentary  origin,  I resorted  in  my  previous  report,  in  order  to  explain  the 
similarity  in  the  composition  ofithe  schists  with  the  massive  diorites,  to  the  hypoth- 
esis of  a secondary  fusion  of  the  lower  beds  of  sediments  nearest  to  the  focus  of  cen- 
tral heat,  and  subsequent  injection  of  the  fused  part  into  the  folds  and  fissures  of 
the  remainder  of  the  strata,  simultaneously  also  the  molten  mass  to  have  been  forced 
into  the  fissures  and  crevices  of  the  adjoining  granite.  I have  since  lost  much  of  ray 
faith  in  this  supposition,  since  I have  convinced  myself  that  schistose  structure  is 
not  necessarily  the  result  of  aqueous  sedimentation,  but  that  cooling  eruptive  masses 
under  circumstances  can  assume  a schistose  form.  * * * I am  inclined  to  suppose 

that  these  schists  so  intimately  associated  with  massive  diorite  beds  are  a product  of 
their  decomposition,  under  circumstances  favoring  the  schistose  arrangement  of  the 
molecules,  or,  to  speak  in  more  definite  terms,  are  a modified  form  of  these  eruptive 
masses,  and  do  not  refer  to  former  sedimentary  deposits. 

My  examinations  of  the  Marquette  region,  made  at  different  times  in 
the  summers  of  1883,  1886,  and  1887,  have  served  to  convince  me  thus 
far  of  the  correctness  of  the  views  of  most  of-  the  geologists  who  have 
examined  the  region  with  regard  to  the  inferior  position  of  the  rocks  of 
the  greenstone-schist  area  to  the  remainder  of  the  stratiform  rocks. 
They  have  also  served  to  impress  me  strongly  with  the  probable  cor- 
rectness of  the  view  which  would  make  at  least  some  granitic  rocks  sub- 
sequent in  point  of  time  to  the  greenstone  schists  themselves,  since  the 
latter  are  so  intricately  penetrated  by  granitic  bosses  and  dikes  in  their 
more  northern  portions. 

I have  also  seen  enough  to  make  me  confident  that  the  dike  masses 
which  cut  the  greenstone  schists  of  this  area  are  of  wholly  subsequent 
date  to  the  schists,  and  indeed  are  equivalent  in  point  of  time  to 
those  intruded  sheets  and  masses  which  lie  within  the  overlying  de- 
trital  iron-bearing  series.  On  the  other  hand,  £ have  seen  some  reason 
to  suspect  that  nearly  all  previous  geologists  have  been  mistaken  in 
considering  the  rocks  of  the  greenstone- schist  area  as  belonging  within 
the  same  great  geological  period  as  that  which  holds  the  remainder  of 
the  stratiform  rocks  of  the  region.  In  other  words,  it  thus  far  appears 
to  me  that  there  is  good  reason  to  believe  that  these  greenstone  schists 
along  with  the  granites,  gneisses,  etc.,  form  a portion  of  the  basement 
upon  which  the  overlying  detrital  iron-bearing  series  was  once  horizon- 
tally and  unconform  ably  spread.  That  they  do  not  constitute  the  con- 
formably underlying  basement  beds  of  that  series  is  suggested  by  a 
glance  at  the  map  (PI.  I),  from  which  it  will  be  seen  that  they  do  not 
everywhere  appear  between  the  granite  areas  and  the  detrital  rocks 
themselves,  the  granite  at  times  coming  in  contact  with  them,  and  again 
with  the  higher  stratiform  horizons.  But  this  anomalous  arrangement 

1 Geological  Ileport  on  the  Upper  Peninsular  of  Michigan,  exhibiting  the  progress  of  the  work 

from  1881  to  1884. 


20 


GREENSTONE  SCHIST  AREAS  OF  MICHIGAN. 


[BULL.  62. 


might  possibly  be  explained  by  the  eruptive  nature  of  the  granite, 
which,  since  eruptive,  would  come  up  indifferently  at  any  horizon  of 
the  rocks  intruded  by  it.  However,  that  the  granite  is  not  newer  than 
those  stratified  rocks  which  overlie  the  greenstone  schists  there  appears 
very  excellent  proof.  At  a number  of  points  where  the  detrital  beds, 
which  form  the  basement  members  of  the  iron-bearing  series  proper, 
come  in  contact  with  the  granite,  they  contain’  its  debris  in  a very  notable 
fashion,  while  they  are  entirely  devoid  of  granitic  veins,  such  as  occur 
where  the  greenstone  schists  come  into  contact  with  the  granite.  If, 
then,  the  granites  are  of  one  general  age,  it  appears  manifest  that  they 
are  newer  than  the  greenstone  schists,  but  older  than  the  overlying 
strata.  Moreover,  there  are  several  points  on  the  contact  line  between 
the  detrital  rocks  of  the  iron-bearing  series  and  the  underlying  green- 
stone schists,  where  a conglomerate  is  to  be  seen,  in  which  are  included 
not  only  numerous  granitic  fragments,  but  also  large  sized  pieces  of  the 
greenstone  schists  themselves. 

Since  the  occurrence  of  these  basal  conglomerates  is  a matter  of  so  im- 
portant a bearing  on  the  geologic  structure  of  this  region,  it  is  desira- 
ble that  the  points  of  their  occurrence  should  be  briefly  indicated  here. 
Beginning  with  the  south  side  of  the  main,  or  southern  area  of  the  iron- 
bearing series,  indicated  on  the  accompanying  sketch  map,  it  may  be 
noted  in  the  first  place  that  at  several  points  along  the  contact  line 
in  Secs.  1,  2,  3,  4,  and  5,  T.  47  N.,  R.  25  W.,  the  basal  quartzite  of  the 
detrital  series,  which  is  in  general  made  up  almost  completely  of  quartz 
fragments  cemented  by  a siliceous  matrix,  takes  on  a peculiar  charac- 
ter, containing  at  times  a large  quantity  of  pinkish  orthoclase,  along 
with  a good  deal  of  sericitic  mica.  This  peculiar  rock  was  regarded  by 
Dr.  Rominger  as  having  been  altered  from  the  quartzite  by  its  contact 
with  the  more  recently  erupted  granite.  A study  of  the  thin  sections, 
however,  reveals  the  completely  fragmental  nature,  not  merely  of  the 
quartz,  but  of  the  feldspar  pieces,  while  the  sericitic  ingredient  appears 
to  have  arisen  from  an  immediate  alteration  of  the  feldspar  fragments. 
These  feldspathic  fragments,  as  also  the  quartz  mingled  with  them,  are 
of  the  kinds  characteristic  of  granite,  and,  moreover,  are  entirely  iden- 
tical with  those  occurring  in  the  granite  with  which  this  peculiar  rock 
is  in  contact.  Southwest  of  Goose  Lake,  however,  in  Secs.  21  and  22, 
T.  47,  R.  26  W.,  there  are  much  more  obvious  occurrences  of  gran- 
itic debris.  In  the  lower  detritals  of  the  iron-bearing  series  near  the 
southwest  quarter  of  section  22  may  be  seen  layers  of  fragmental  quartz 
slate  holding  seams  of  granitic  pebbles;  while  in  the  southeast  quarter 
of  the  same  section  contacts  are  seen  between  the  fragmental  quartzite 
and  masses  of  the  granite,  the  quartzite  at  the  contact  being  crowded 
with  bowlders  and  fragmental  material  of  all  sizes  derived  from  the 
granite.  It  is  not  evident  whether  the  granitic  masses  here  seen  are 
brought  to  view  by  a fold  of  the  strata,  or  are  directly  connected  at 
surface  with  the  main  granitic  mass  lying  to  the  southeast  of  them,  the 


IRVING.] 


BASAL  CONGLOMERATES  NEAR  MARQUETTE. 


21 


exact  outlines  of  the  areas  occupied  by  different  rocks  in  this  vicinity 
having  never  been  traced.  These  occurrences  were  noted  by  Dr.  Rom- 
inger,1  who  also  describes  similar  ones  as  obtaining  in  the  southwest- 
ern x>ortion  of  the  same  township.  It  should  also  be  said  that,  at 
numerous  points  along  this  line,  the  quartzite  contains  pebbly  beds  in 
which  the  pebbles  are  of  a quartzite  whose  microscopic  features  prove 
to  be  those  so  well  known  as  characteristic  of  the  quartz  of  granite. 

Turning  now  to  the  northern  line  of  the  same  area  we  may  note  first 
the  conglomerate  to  be  seen  on  the  side  of  the  so-called  State  Road, 
running  west  from  Marquette  at  a point  near  the  west  line  of  the  SW. 
J of  the  SE.  J sec.  29,  T.  48  R.  25  W.  This  is  exactly  on  the  line 
between  the  greenstone- schist  area  and  the  area  occupied  by  the  detrital 
rocks,  which  just  here  are  thinly  banded  slates,  standing  vertical  or 
even  overturned  slightly  so  as  to  dip  to  the  northward  and  to  lie  in  gen- 
eral conformity  to  the  cleavage  of  the  greenstohe  schists  immediately 
north.  These  slates,  whose  lithological  character  is  one  very  commonly 
met  with  at  the  base  of  the  iron-bearing  series  in  many  different  por- 
tions of  the  Lake  Superior  region,  are  proved  by  the  thin  sections  to 
be  quite  beyond  question  water-formed  detritals  and  at  the  same  time 
to  present  a most  striking  contrast  with  the  hornblendic  and  chloritic 
greenstone  schists  lying  immediately  north  of  them.  This  contrast, 
however,  though  very  distinct  in  the  thin  section,  is  by  no  means  so 
pronounced  in  the  hand-specimens  which,  though  one  sees  that  they  are 
of  two  different  natures,  might  nevertheless  be  readily  takeu  to  be  all 
of  the  same  origin.  At  the  point  indicated  the  fragmental  slates  become 
crowded  with  large  and  small  fragments  of  granite,  quartz,  and  green 
schist,  the  quartz  pebbles  usually  being  of  rather  small  size,  while  those 
of  granite,  which  are  the  most  numerous,  are  well  rounded  and  reach  as 
much  as  two  feet  in  diameter.  The  green  schist  pebbles,  on  the  other 
hand,  are  not  so  plentiful,  but  are  still  abundant  and  of  all  sizes,  from 
the  smallest  particles  up  to  pieces  a foot  across.  The  larger  schist 
pieces  are  somewhat  rounded,  but  in  the  main  they  are  all  far  less  so 
than  the  fragments  of  granite  and  quartz.  The  thin  sections  cut  from 
the  matrix  of  the  rock  show  that  it  is  completely  of  a detrital  nature. 
On  the  north  side  of  Teal  Lake,  at  both  eastern  and  western  extremities, 
are  found  other  conglomerates,  in  one  case  holding  only  quartz  pebbles, 
and  in  the  other  case  pebbles  not  only  of  quartz,  but  of  greenish  schists 
as  well. 

Turning  our  attention  now  to  the  northern  one  of  the  two  detrital 
areas  indicated  on  the  sketch-map  herewith  (PI.  I),  I may  note  the  oc- 
currence at  a number  of  points  along  its  southern  margin  of  conglom- 
eratic layers  of  quartzite  and  sandstone,  in  which  are  contained  peb- 
bles of  white  quartz,  which  pebbles  are  at  times  identical  in  microscopic 
and  macroscopic  appearance  with  the  quartz  of  certain  seams  in  the 
greenish  schists  (as,  for  instance,  on  the  west  line  of  Sec.  20,  T.  48  N.,  R. 


1 Geol.  Survey,  Michigan,  vol.  4,  1881,  pp.  62,  63. 


22  GREENSTONE  SCHIST  AREAS  OF  MICHIGAN.  [bull.  62. 

27  W.),  or  with  that  of  the  granite  (as,  for  instance,  near  the  middle  of 
the  south  half  of  Sec.  17,  T.  48  N.,  R.  26  W.),  against  which  different 
rocks  the  quartzites  rest  indifferent  places.  Near  the  middle  of  Sec.  21, 
T.  48  N.,  R.  27  W.,  the  quartzite,  resting  here  against  certain  agglom- 
erate green  schists,  contains  not  only  fragments  of  quartz  like  that  of 
numerous  seams  in  the  green  schists,  but  also  pieces  of  the  green  schists 
themselves,  which  in  some  cases  are  several  inches  in  diameter. 

But  the  most  striking  occurrences  of  basal  conglomerates  upon  the 
edges  of  this  area  of  detrital  rocks  are  those  to  be  met  with  in  the 
northern  and  western  portions  of  T.  49  N.,  R.  28  W.  One  of  these  places, 
to  which  my  attention  was  first  drawn  by  Mr.  C.  E.  Wright,  the  state 
geologist  of  Michigan,  is  on  the  northwestern  shore  of  Silver  Lake,  in 
the  SE.  J of  the  Is  W.  J of  Sec.  8.  Rising  abruptly  all  along  the  north- 
ern side  of  this  lake  is  a bold  ridge  of  granite  with  which  are  associated 
several  kinds  of  schistose  rocks,  very  prominent  among  which  is  a fine- 
grained green  schist  entirely  analogous  in  general  appearance  to  the 
greenstone  schists  which  form  the  special  subject  of  this  paper.  At 
the  particular  point  to  which  attention  is  now  directed,  this  granite  pro- 
trudes in  places  into  the  lake  in  low,  shelving  ledges,  facing  which,  and 
lying  within  the  cracks  of  which,  is  a black  cherty  slate.  Following 
the  shore  along  to  the  southwestward  from  these  exposures,  the  cherty 
slate  is  found  more  largely  developed,  occupying  a large  hollow  in  the 
surface  of  the  granite,  and  becoming  crowded  with  its  fragments  of  all 
sizes,  from  a fine  detritus  up  to  pieces  two  feet  in  length.  These  frag- 
ments, though  prevailingly  subangular  to  angular  in  outline,  generally 
present  some  evidence  of  water- wearing.  Many  of  them  are  quite 
gneissoid  in  structure,  while  others  are  more  granitic,  two  principal 
phases  being  thus  presented.  The  thin  sections  made  from  the  speci- 
mens selected  on  the  ground  as  characterizing  these  two  phases  of  peb- 
bles, and  also  the  granitic  and  gneissoid  phases  of  the  granite  against 
which  the  conglomerate  rests,  show  the  entire  indentity  of  the  frag- 
ments and  the  massive  granite.  In  addition  to  the  granite  fragments 
are  rarer  ones  of  white  quartz,  these  occasionally  being  of  some  size, 
and  others  of  a greenish  schist  entirely  analogous  to  that  green  schist 
which  occurs  here  in  situ  along  with  the  granite.  The  matrix  of  this 
conglomerate  is  a dark  gray  to  nearly  black,  carbonaceous,  cherty  slate, 
which  in  the  thin  section  shows  a predominating  quantity  of  a cherty, 
chemically  deposited  silica,  with  which  are  mingled  varying  proportions 
of  fragmental  material,  this  fragmental  material  being  composed  of 
pieces  of  quartz  and  feldspar,  and  again,  when  the  pieces  become  coarser, 
of  a granite  in  which  these  same  minerals  are  attached  to  each  other. 
At  times,  as  is  so  commonly  the  case  among  the  cherty  rocks  of  the 
iron- bearing  series  generally,  throughout  the  Lake  Superior  region,  there 
is  a brecciated  condition  in  this  slaty  matrix  itself ; that  is  to  say,  irregu- 
lar, angular  pieces  of  the  carbonaceous  cherty  material  are  cemented 
together  by  a matrix  of  the  same  substance.  Quite  similar  occurrences 


IRVING.] 


AGE  OF  THE  GRANITES, 


23 


are  met  with  near  the  center  of  Sec.  19,  of  the  same  township,  where 
black  cherty  slate  and  quartzite  lie  upon  the  east  and  south  flanks  of  a 
bold  hill  of  granite  ; both  slate  and  quartzite,  and  particularly  the  lat- 
ter, being  crowded  with  fragments  of  the  granite,  which  range  from 
small  pebbles  up  to  pieces  a foot  or  more  in  diameter,  the  smaller  sized 
pebbles  being  usually  quite  well  rounded,  while  the  larger  fragments 
are  subangular  to  angular. 

Such  occurrences  as  these,  when  considered  in  connection  with  the 
manner  in  which  the  granite  penetrates  the  greenish  schists  and  is  in- 
volved with  them,  seem  to  render  necessary  the  belief  that,  while  it  is 
plainly  younger  than  the  green  schists,  it  is  nevertheless  greatly  older 
than  the  overlying  detrital  rocks ; and  more  than  this,  that  when  the 
latter  rocks  were  spread,  the  granites  and  greenstone  schists  together 
had  already  suffered  disturbance  and  deep  denudation.  It  does  not 
appear  possible  to  escape  this  conclusion  by . supposing  that,  since 
granite  and  greenstone  schists  are  eruptives,  they  may  have  furnished 
fragments  to  almost  contemporaneous  sedimentary  deposits ; for,  in 
the  first  place,  both  the  greenstone  schists  and  the  gneissoid  granite 
must  have  receiv'ed  their  schistosity  before  yielding  the  fragments. 
Moreover,  whatever  may  have  been  the  depth  at  which  the  schistose 
rocks  were  first  formed,  the  granitic  masses  which  intruded  them,  ac- 
cording to  all  the  later  developments  and  doctrines  of  petrography, 
must  have  been  crystalized  in  depth,  and  must  therefore  have  had  re- 
moved from  over  them  great  masses  of  materials  before  yielding  frag- 
ments to  wave  action.  In  this  connection  attention  should  be  drawn 
to  the  fact  tbat  there  are  evidently  granitic  rocks  of  two  different  ages 
in  the  great  granitic  areas  of  the  Marquette  region  ; because  dikes  of  a 
fine  grained,  reddish  granite  are  frequently  met  with  cutting  the  other 
granite,  which  may  be  either  gneissoid  or  not.  These  later  granites, 
which  appear  to  be  of  relatively  small  extent  compared  with  the  main 
mass,  may  perhaps  have  been  even  later  in  time  of  formation  than  the 
detrital  rocks  themselves.  It  seems  probable  that  to  these  later  granitic 
eruptions  we  should  refer  certain  Tare  quartz-porphyry  dikes,  and  such 
very  rare  granitic  dikes  as  that  which  is  seen  near  Metropolitan,  in  the 
Felch  Mountain  district,  intersecting  a ferruginous  schist  of  the  iron- 
bearing series  itself. 

On  the  whole,  then,  accepting  Prof.  Williams’s  conclusions  as  to  the 
surface  origin  of  most  of  the  greenstone  schists  of  the  Marquette 
region,  I should  suppose  that,  after  the  accumulation  of  these  rocks  to 
the  thickness  of  several  thousand  feet,  they  were  intruded  by  granitic 
bosses.  These  bosses  perhaps  may  have  been  merely  softened  portions 
of  the  underlying  gueissic  basement,  which  indeed  may  be  represented 
in  an  unaltered  condition  in  portions  of  the  granitic  areas  themselves, 
for  all  that  has  yet  been  determined  to  the#  contrary.  Subsequent 
mountain-making  movements  brought  about  the  folding  and  altera- 
tion of  these  enormous  sheets  of  eruptive  material,  now  represented  by 


24 


GREENSTONE  SCHIST  AREAS  OF  MICHIGAN. 


[BULL.  62. 


the  greenstone  schists.  Following  this  was  the  great  denudation 
which  brought  to  light  the  previously  buried  granitic  masses.  This 
erosion  was  followed  in  turn  by  the  accumulation  in  the  usual  horizon- 
tal position  of  the  iron-bearing  detrital  series,  whose  folding  and  erosion 
were  still  later  processes.  And  yet  this  folding  and  erosion  all  pre- 
ceded the  deposition  of  the  horizontal  Cambrian  sandstones  of  the 
region. 

The  entire  similarity  which  is  shown  by  Prof.  Williams  to  obtain  be- 
tween the  great  dikes  of  diabasic  greenstone  which  traverse  the  green- 
stone schist  area,  and  the  sheets  of  eruptive  greenstone  which  are  in- 
cluded within  the  iron-bearing  series,  furnishes  a further  confirmation 
of  these  conclusions.  For  the  latter  greenstones  are  in  large  measure 
directly  interstratified  with  the  sedimentary  layers  of  the  iron-bearing 
series,  following  the  bending  of  its  layers;  so  that  even  if  these  green- 
stones are  in  the  nature  of  intruded  sheets,  it  seems  necessary  to  be- 
lieve that  their  intrusion  took  place  before  the  folding  of  the  iron-bear- 
ing series.  Now,  the  corresponding  dikes  in  the  greenstone-schist  area 
were  evidently  intruded  subsequent  to  the  production  of  the  schis- 
tosity  of  the  intruded  rocks.  If,  then,  these  are  facts,  the  time  when 
the  iron-bearing  series  was  folded  was  very  much  subsequent  to  that 
time  at  which  the  greenstone  schists  received  their  schistosity.  It  has 
been  mentioned  that  the  schistose  structure  of  these  greenstones  at 
times  corresponds  with  the  bedding  structure  of  the  iron-bearing 
series.  But  quite  frequently  there  is  no  such  correspondence,  the  beds 
of  the  latter  series  being  noticeably  at  relatively  lower  angles  when 
compared  with  the  vertical1  schistose  structures  of  the  greenstone 
schists  themselves. 

Such  correspondence  in  some  places  and  lack  of  correspondence  in 
others  are  easily  enough  explicable  upon  the  views  that  I have  ad- 
vanced. However,  there  is  good  reason  to  think  that  at  the  time  of  the 
folding  of  the  iron-bearing  series,  the  greenstone  schists  received  a sec- 
ond squeezing,  which  developed  further  alterations  and  further  schis- 
tosity. The  later  dikes  just  alluded  to  as  penetrating  the  green  schists 
are  at  times  rendered  somewhat  schistose,  though  far  less  markedly  so 
than  are  the  rocks  which  they  intrude.  The  same  is  true  with  the  green- 
stones that  are  intercalated  in  the  iron-bearing  series,  where  somewhat 
schistose  phases  are  found.  The  structure  of  these  last-named  schis- 
tose phases,  as  also  the  occasional  slaty  cleavage  seen  in  the  detrital 
layers  of  the  iron-bearing  series,  where  it  is  very  strongly  folded,  cor- 
respond in  general  direction,  as  would  be  expected,  with  the  schistose 
structure  of  the  green  stone- schist  areas. 

The  geology  of  that  portion  of  the  Menominee  region  which  has  been 
especially  under  study  in  the  present  connection,  is  indicated  by  the 
outline  map,  Plate  II.  Here,  again,  we  find  a series  of  detrital  iron- 
bearing rocks,  lying  between  great  areas  of  granite  and  gneiss.  The 
iron-bearing  rocks  are  generally  quite  closely  like  those  of  the  Mar- 


THE  LIBRARY 
OF  THE 

UNIVERSITY  OF  ILLINOIS 


T.  38  N 


R. UFOLOGICAL  SURVEY- 


Antoine 


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Yieinne: 

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*.  "v , «\  t,  V%f.  >- 

WimiM 


ARCHEAN. 

Granite  and  Gneiss.  Greenstone  Schists 


OUTLINE  GEOLOGICAL  MAP  C 

Compiled,  bv  R.D.  Irving  from  maps  by  T.B.B rooks, 

Seal 

.0  .3  _ 


ALGONKIAN 

Iron  Bearing  Series. 

•tritals, Limestones  & Femicjinmis  . 
Sri  lists.) 

A i 


CAMBRIAN. 

j A_ y 

Potsdam  Sandstone . 


| 


THE  MENOMINEE  IRON  REGION. 


AVriijht  and  ('.Roniinger  and  lrom  original  observations. 

f miles. 

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080 


T.39N. 


THE  LIBRARY 
OF  THE 

UNIVERSITY  OF  ILLINOIS 


lKVTN'G,] 


GREENSTONE  SCHISTS  ON  THE  MENOMINEE. 


25 


quette  region,  the  only  important  differences  being  the  very  great  rar- 
ity of  greenstone  intrusions,  and  the  very  much  more  closely  crumpled 
condition  which  the  rocks  here  present.  In  the  same  region  are  two 
belts  of  greenstone  schists  closely  analogous  in  general  appearance 
with  those  of  the  Marquette  region.  The  southern  one  of  these  borders 
for  a long  distance  the  southern  granite  area,  separating  the  granite 
from  the  detrital  rocks  further  north.  The  inclination  of  the  schistosity 
of  the  greenstone  schists  is  almost  vertical,  there  being  generally  a 
slight  southern  departure  from  verticality.  Very  high  southern  dips, 
often  approaching  verticality,  also  prevail  among  the  layers  of  the  de- 
trital succession  itself,  although  here  frequently  occur  reverse  dips  to 
the  northward,  often  at  a flatter  angle. 

The  first  geologists  who  appear  to  have  noted  the  Menominee  rocks 
are  Foster  and  Whitney  and  Charles  Whittlesey,  as  quoted  in  Foster 
and  Whitney’s  work.1  By  these  writers  all  of  the  Menominee  strati- 
form rocks,  so  far  as  they  were  encountered  in  the  rapid  trips  by  canoes, 
which  were  at  that  time  the  only  means  of  traversing  the  country, 
were  classed  together  under  the  general  name  of  Azoic  slates.  How- 
ever, the  exposures  of  greenstone  schists,  which  are  met  with  at  Twin 
Falls,  Upper  (Big)  and  Lower  (Little)  Quinnesec  Falls  and  Sturgeon 
Falls,  appear  to  be  directly  referred  to  as  intercalations  of  “ Azoic 
slates  and  traps ; ” so  that,  while  no  opinion  was  expressed  as  to  their 
stratigraphic  relations  to  the  other  rocks  of  the  region — beyond  what  is 
indicated  in  general  statements  as  to  the  greater  recency  of  all  the 
granitic  masses  of  the  region  as  compared  with  the  schistose  and  slaty 
rocks — it  appears  plain  that  these  geologists  looked  upon  the  rocks 
now  included  under  the  term  of  greenstone  schists  as  partly  eruptive 
and  partly  sedimentary. 

The  same  conclusion  as  to  the  origin  of  these  rocks  appears  to  have 
been  reached  by  Gredner,  who  published  an  account  of  this  region  in 
I860,2  after  having  been  some  time  on  the  ground  as  an  assistant  to 
Prof.  R.  Pumpelly  in  a private  economic  examination  of  the  lands  of 
the  Lake  Superior  Ship  Canal  Company.  On  account  of  the  slight  de- 
parture from  verticality  towards  the  south;  on  account  of  the  schistose 
structure  of  the  rocks  exposed  at  the  several  falls  of  the  Menominee, 
which  rocks  he  describes  under  the  general  term  of  “ Dioritic  Series’ 
and  “Talcky  Clay  Slate,”  and  because  of  the  prevalence  of  similar 
southern  dips  among  the  detrital  iron-bearing  rocks  farther  north, 
Credner  considers  the  former  rocks  as  constituting  the  highest  portion 
of  the  entire  succession  of  the  region.  That  there  existed  to  the  south 
of  these  rocks  another  mass  of  granite  does  not  appear  to  have  been 
realized  by  Credner. 

T.  B.  Brooks,  who  followed  Credner  in  the  Menominee  region  and 

* Geological  Survey  of  the  Lake  Superior  Land  District,  vol.  2,  pp.  24-31.  See  also  general  soctlon 
of  the  Lake  Superior  region  in  atlas  to  the  same  volume. 

2 Die  vorsilurischen  Gebilde  dor  oberen  Halbinsel  von  Michigan  in  Nord-Amorika.  Zeitschr. 
Deutsch.  geol.  Gesell.,  Berlin,  18G9,  vol.  21,  pp.  516-554. 


26  GREENSTONE  SCHIST  AREAS  OF  MICHIGAN.  [bull.  62. 

who  published  a brief  account  in  the  reports  of  the  Geological  Survey  of 
Michigan1,  appears  to  have  agreed  with  that  geologist  with  regard  to 
the  relatively  high  position  in  the  series  of  the  greenstone  schists  of 
the  Menominee  River.  Subsequently  the  same  geologist,  assisted  by 
0.  E.  Wright,  was  engaged  in  a more  minute  examination  of  this 
region  on  the  part  of  the  Wisconsin  State  Geological  Survey,  publish- 
ing a somewhat  elaborate  report  in  1880.2  In  this  report  very  many 
more  facts  are  given  than  were  ever  known  before,  all  exposures  seen 
being  very  accurately  and  carefully  indicated  upon  the  accompanying 
maps.  This  detailed  work,  however,  does  not  appear  to  have  altered 
Brooks’s  opinion  as  to  the  relatively  high  position  in  the  Menominee 
series  of  the  greenstone  schists  now  especially  under  consideration, 
although  it  appears  that  he  would  now  correlate  them  with  still  higher 
layers  of  the  Marquette  series  rather  than  with  those  to  which  he 
had  previously  referred  them.  As  to  the  origin  of  the  greenstone 
schists,  Brooks  would  seem  to  have  regarded  them  at  first  as  all  sedi- 
mentary; at  all  events  when  the  Michigan  report  referred  to  was 
written.3  Later,  however,  he  appears  to  have  been  disposed  to  separate 
from  the  rest  certain  diabases  as  eruptive,  thus  coming  nearly  to  the 
same  conclusion  as  that  reached  by  Credner.4  To  convey  Brooks’s  con- 
ception of  the  structure  of  this  region  more  clearly,  there  are  given  here 
two  sections,  constructed  from  general  sections  given  by  him  upon 
Plates  27  and  29  of  the  atlas  to  the  Geology  of  Wisconsin.  The  granitic 

jswr  JV"JE. 


Fig.  1.  Hypothetical  section  of  the  Menominee  region  in  the  vicinity  of  Quinnesec,  according  to 
Brooks;  I,  Sericitic  slates;  II,  quartzite  ; V,  limestone;  VI,  the  great  iron  horizon;  XIV,  quartzite  ; 
XV  to  XIX,  greenstone  schists,  etc. ; XX,  Huronian  granite;  P,  Potsdam  sandstone.  Scale  13,000 
feet  to  the  inch. 

and  gneissic  rocks  to  the  north  Brooks  regarded  as  having  formed  part 
of  the  ancient  Laurentian  basement  upon  which  all  of  the  slates  and 
schists  were  subsequently  piled.  From  this  northern  granite  to  the 
granite  on  the  south  side  of  the  Menominee  he  looked  upon  the  entire 
succession  as  an  ascending  one,  though  admitting  certain  bowings  of 
the  strata.  The  southern  granite,  as  to  whose  sedimentary  or  eruptive 
origin  he  appears  to  have  been  doubtful,  he  places  as  the  summit  mem- 
ber of  the  Huronian  series.  The  entire  succession  he  divides  into  three 
portions,  beginning  below  or  to  the  north,  as  follows  : Lower  Huronian, 

1 Geol.  Michigan,  vol.  1,  1873,  pp.  157-182.  See  also  atlas  to  the  same,  PI.  4. 

2 Geol.  Wisconsin,  vol.  3,  1880,  pp.  430-663  ; also  atlas,  Pis.  28-30. 

8 Geol.  Michigan,  vol.  1,  1873. 

4Geol.  Wisconsin,  vol.  3,  1880,  p.  521. 


IRVING.} 


OBSERVATIONS  OF  BROOKS  AND  ROMINGER. 


27 


5,200  feet ; Middle  Huronian,  3,100  feet;  Upper  Huronian,  10,700  feet; 
making  in  all  a maximum  thickness  of  19,000  feet  beneath  the  upper  or 
southern  granite.  The  surface  distribution  of  the  uppermost  of  these 
three  divisions  corresponds  almost  exactly  with  the  areas  of  greenstone 
schists  indicated  upon  the  outline  map  herewith  (PI.  II).  The  more  north* 


HURONIAN 

Fig.  2.  Hypothetical  section  of  the  Menominee  region  in  the  vicinity  of  Twin  Falls,  according  to 
Brooks.  Scale  13,000  feet  to  the  inch.  Letters  and  shadings  have  the  same  significations  as  in  Fig.  1. 


ern  area  of  greenstone  schists,  namely,  that  which  is  sectioned  by  the 
Menominee  river  at  Twin  Falls,  is  made  on  Brooks’s  structural  sketches 
to  be  brought  to  view  by  a synclinal  depression  of  tbe  strata.  For  this 
view  of  the  structure  of  the  region  there  never  was  any  other  support 
than  the  very  slight  departure  from  verticality  towards  the  south  of 
the  schistose  structure  of  the  southern  greenstone  schists  and  a pre- 
vailing similar  inclination  in  the  detrital  iron  bearing  series  proper. 
No  contacts  of  the  different  kinds  of  rocks  were  observed  to  support 
Brooks’s  hypotheses  as  to  the  relatively  high  position  of  the  greenstone 
schists  and  southern  granite,  between  which  and  the  other  stratiform 
rocks  there  is  indeed  usually  a wide  belt  of  country  without  exposures. 
On  the  other  hand,  the  extraordinary  similarity  of  these  greenstone 
schists  to  those  which  Brooks  regarded  as  underlying  the  entire 
Marquette  series  appears  to  have  been  disregarded,  as  also  was  the 
complete  similarity  between  the  northern  and  southern  granites,  and 
again  between  the  contact  of  the  southern  granite  with  the  green- 
stone schists  next  to  it,  and  the  corresponding  contact  in  the  Marquette 
region. 

Itominger,  who  followed  Brooks  in  the  Menominee  region  in  1880 
and  published  an  account  of  his  observations  in  1881,  appears1  to  have 
realized  very  vividly  the  difficulties  met  with  in  accepting  Brooks’s 
structural  hypothesis.  He  represents  all  of  the  greenstone  schists  of 
the  region  as  belonging  at  the  base  of  the  entire  stratiform  series,  and 
as  equivalent  in  position  and  nature  with  the  similar  rocks  of  the  Mar- 
quette region.  The  northern  and  southern  granites  Kominger  looks 
upon  as  the  same,  and  as  intrusives  of  a date  later  than  the  accumulation 
of  the  entire  stratiform  succession.  As  to  origin,  he  evidently  looked 
upon  the  greenstone  schists  as  altered  sedimentaries,  assigning  the 
relatively  great  alteration,  which  on  this  view  they  must  be  assumed 
to  have  undergone,  to  the  action  of  the  later  granitic  bosses;  in  which 


•Geol.  Survey  Michigan,  vol.  4,  1881,  pp.  157-241. 


28 


GREENSTONE  SCHIST  AREAS  OF  MICHIGAN. 


[BULL.  62. 


view  he  fails  quite  to  explain,  as  he  does  in  the  case  of  the  Marquette 
region,  how  the  southern  granite  of  the  Menominee  area  should  have 
produced  so  great  alterations,  while  that  on  the  north  comes  in  contact 
with  wholly  unaltered  detrital  rocks,  to  which  moreover,  as  Brooks  had 
previously  shown,  it  furnishes  an  abundance  of  detrital  material.  Un- 
fortunately, though  describing  carefully  very  many  exposures  not  re- 
corded on  Brooks’s  map,  Bominger  gives  no  sections  indicative  of  his 
views  as  to  structure.  Just  what  his  ideas  were  in  this  respect  it  is 
not  easy  to  make  out  from  his  descriptions,  but  it  appears  evident  that 
with  him  the  greenstone  schists  lie  at  the  base  of  the  succession  5 that 
they  are  next  succeeded  in  order  by  those  slates  which  lie  about  Lake 
Hanbury;  that  these  are  succeeded  by  the  great  ore  horizon,  and  this 
by  the  great  limestone  bed  of  the  region  with  a thickness  of  a thousand 
feet  and  more.  Thus  he  reverses  entirely  the  succession  as  given  by 
Brooks,  and  as  it  appears  in  nature  so  far  as  the  limestone  and  ore 
belts  are  concerned.  What  strati  graphical  position  Rominger  would 
give  to  those  great  masses  of  quartzite  which  lie  adjacent  to  the  northern 
granite  in  Menominee  belt  I have  not  been  able  to  understand  distinctly 
from  his  descriptions.  The  Twin  Falls  greenstone  schists  he  would 
place  along  with  the  Quiunesec  series  at  the  base  of  the  entire  succes- 
sion, bringing  them  to  the  surface  by  an  anticlinal  instead  of  a syn- 
clinal fold,  such  as  is  resorted  to  by  Brooks.  The  following  paragraphs 
are  quoted  from  Rominger,1  as  indicative  of  his  views  upon  these  points : 

A superposition  of  the  diorite  formation  on  the  Lake  Hanbury  rock  series,  which 
adjoins  in  the  whole  length  of  the  Menominee  valley  from  the  upper  Quiunesec  Falls 
to  the  Sturgeon  Falls,  asserted  by  Major  Brooks,  is  not  observable ; the  nearly  verti- 
cal strata  of  both  formations  are  even  never  seen  in  contact.  There  is  always 
quite  a large  covered  interval  between  them.  The  nearest  exposures  of  the  two  groups 
are  observable  in  Sec.  26,  T.  39,  R.  29,  where,  in  the  center  of  the  section,  a hill  is  formed 
of  the  vertical  ledges  of  ferrugino-siliceous  flagstones  and  slaty  beds  representing  the 
Lake  Hanbury  series,  and  about  two  or  three  hundred  steps  from  these  exposures  we 
find  on  the  south  side  of  the  road  to  Menominee  small  hillocks  of  diorite.  * * * 

My  reasons  for  holding  the  dioritic  rocks  south  of  the  iron  formation  as  older 
than  the  latter  are  based  on  the  lithological  similarity  of  this  formation  with 
the  dioritic  group  of  the  Marquette  district  and  on  the  degree  of  metamorphism  ex- 
hibited by  the  two  groups,  the  dioritic  and  the  iron-bearing.  In  the  great  succession 
of  strata  commencing  with  the  Hanbury  slate  group  and  upward  we  rarely  find  a 
bed  so  much  altered  that  its  sedimentary  structure  is  altogether  obsolesced,  and  the 
majority  of  the  strata  shows  it  very  plain,  while  in  the  dioritic  rocks,  considered  to  be 
the  younger,  a stratified  structure  is  also  recognizable,  but  not  one  of  these  thousands 
of  feet  of  ledges  exhibits  its  original  sedimentary  lamination  with  any  degree  of  dis- 
tinctness like  the  others  ; they  have  evidently  been  transformed  under  cooperation 
of  heat  and  partially  brought  into  a plastic  condition,  which  is  shown  by  the  ex- 
treme corrugation  and  mode  of  intermixture  of  those  rock  masses,  of  which  effects  the 
other  rock  groups  do  not  exhibit  near  as  high  a degree.  It  would  be  very  strange, 
then,  if  the  lowest  beds  nearest  to  the  focus  of  the  central  heat  should  have  been  so 
much  less  affected  by  these  altering  influences  than  those  pretended  to  be  the  higher 
upper  strata  of  the  rock  crust.  One  might  object : If  the  diorites  are  the  older  beds, 
why  don’t  we  find  them  just  as  well  developed  on  the  north  side  of  the  upheavedbeds 
between  the  quartzite  and  the  granite  ? The  saudy  and  conglomeratic  nature  of 


1 Geol.  Survey  Michigan,  vol.  4.  1881,  pp.  208-210. 


IRVING.] 


OBSERVATIONS  OF  ROMINGER  AND  IRVING. 


29 


many  of  the  strata  of  the  quartzite  and  iron  formation  proves  them  to  be  shore  depos- 
its, while  the  dioritic  group  consists  only  of  the  finer  material  of  deep  sea  deposits, 
which  explains  the  point  in  question.  Moreover,  the  dioritic  rocks  are  not  altogether 
missing  on  the  north  side  of  the  ore-formation,  as  we  can  see  by  the  occurrence  of  the 
6-mile-long  chain  of  diorite  extending  eastward  from  the  Twin  Falls.  A similar  dis- 
crepancy between  the  rocks  underlying  the  ore-formation  on  the  two  opposite  sides 
of  its  exposure  is  seen  in  the  Negaunee  district.  On  the  south  margin,  at  the  Cas- 
cade and  Palmer  mines,  it  rests  directly  on  the  granite,  while  on  the  northern  expo- 
sures the  diorite  underlies  it  in  great  thickness. 

The  equal  dip  of  the  strata  to  the  south  in  these  adjoining  formations  is  not  neces- 
sarily a proof  of  the  younger  age  of  the  most  southern  beds.  The  whole  succession  is 
so  near  to  a vertical  position  that  in  many  instances  it  has  to  be  left  uncertain  which 
way  they  dip,  but  suppose  their  dip  is  conformably  to  the  south ; the  upheaval  of  the 
diorites  by  the  eruption  of  the  still  more  southern  granite  masses  pushing  the  whole 
incumbent  rock-series  north  until  all  tipped  over  is  the  hypothesis  by  which  I explain 
the  order  in  the  succession  of  beds  as  an  inverted  one,  the  seemingly  lowest  beds  being 
actually  the  youngest. 

In  my  own  studies  in  the  Menominee  region,  made  in  the  summers  of 
1883  and  1885, 1 became  early  impressed  with  the  close  similarity  be- 
tween the  greenstone  schists  of  the  Menominee  River  and  those  which 
underlie  the  iron-bearing  series  of  Marquette ; with  the  entire  similar- 
ity between  the  rest  of  the  stratiform  rocks  of  the  region  and  those  of 
the  Marquette  district ; with  the  essential  identity  in  character  of  the 
granite  areas  lying  respectively  on  the  northern  and  southern  sides  of 
the  Menominee  River;  with  the  granitic  intrusions  met  with  in  the  green- 
stone schists  bordering  the  southern  granite,  and  with  the  striking  con- 
trast between  the  nature  of  this  contact  and  that  of  the  northern  gran- 
ite with  the  detrital  rocks  which  border  it  to  the  south.  In  the  latter 
case  the  granite,  instead  of  sending  intrusions  into  the  rocks  which 
rest  against  it,  has  furnished  fragments  to  them,  as  may  be  most  beau- 
tifully seen  at  the  Falls  of  Sturgeon,  Sturgeon  River,  on  the  eastern  side 
of  Sec.  8,  T.  39,  R.  28  W.,  Michigan.1  These  considerations  naturally 

1 For  previous  descriptions  of  the  striking  occurrences  at  the  Falls  of  Sturgeon,  Sturgeon  River, 
see  Credner  in  “Die  vorsilurischen  Gebilde  der  oberen  Halbinsel  von  Michigan,”  Zeitschrift  der 
Deutschen  geologischen  Gesellsehaft.  vol.  21, 1869,  p.  521,  et  seq. ; also  T.  B.  Brooks,  in  Geol.  Wisconsin 
vol.  3, 1880,  pp.  467,  468,  and  Atlas,  PI.  38 ; also,  see  Rominger,  Geol.  Michigan,  vol.  4,  p.  192.  The 
granitic  fragments  at  this  place  occur  in  a fine-grained  slaty  rock,  in  which  there  is  a great  deal  of 
gericitic  material,  which  at  times  gives  the  slate  somewhat  the  look  of  a crystalline  schist.  This  fact, 
along  with  the  slight  inclination  from  the  vertical  towards  the  north,  and  therefore  towards  the  gran- 
ite, which  is  so  largely  exposed  farther  up  the  stream,  led  Credner  to  include  these  conglomeratic  lay- 
ers, along  with  the  granite,  as  Laurentian,  the  great  quartzite  mass  farther  south  being  taken  by  him 
as  the  basement  member  of  the  Huronian.  Brooks,  however,  objects  to  this  conclusion,  considering 
that  the  conglomerates  to  be  seen  at  this  place  are  genuinely  basal  conglomerates,  and  that  they  form 
the  lowest  portion  of  the  Huronian  region.  To  support  this  view,  Brooks  draws  attention  to  the  fre- 
quent arenaceous  nature  of  the  conglomeratic  slates-,  their  ripple-marked  surfaces;  their  generally 
little  altered  appearance ; their  parallelism  of  strike  with  the  admitted  Huronian  beds  farther  south, 
and  the  lack  of  parallelism  between  this  strike  and  such  structures  as  is  to  be  seen  in  tho  granitic  and 
gneissic  rocks  on  the  north.  Rominger’s  description  corresponds  with  that  of  Brooks,  except  that  he 
seems  to  describe  a granitic  mass  or  sheet  as  occurring  interleaved  with  the  conglomerates  themselves, 
a statement  for  which,  in  my  examinations,  I could  find  no  support  whatever.  Rominger,  however, 
to  whom  the  greater  recency  of  all  the  granite  as  compared  with  all  the  stratiform  rocks  was  an  ac- 
cepted conclusion,  explains  the  occurrences  as  he  saw  them  by  the  singular  supposition  that  “we  have 
here  evidently  a series  of  sedimentary  beds,  deposited  on  a granitic  substratum,  which,  during  the  up- 
heaval, became  wedged  in  between  the  plastic  granite  mass,  tilting  and  overlapping  them  locally  so  as 
to  appear  as  tho  lower  beds,”  thus  making  the  same  granite  yield  fragments  to  tho  sedimentaries,  and 
subsequently  intrude  them,  It  should  bo  said  that  the  examinations  of  tho  sovoral  geologists  were 


30 


GREENSTONE  SCHIST  AREAS  OF  MICHIGAN. 


| BULL.  62. 


led  me  to  the  conclusion  that  the  whole  structure  in  this  district  is  sim- 
ilar to  that  already  described  as  obtaining  in  the  Marquette  region, 
namely,  that  the  granitic  masses  had  intruded  themselves  in  the  shape 
of  great  bosses  into  rocks  now  represented  by  the  greenstone  schists, 
after  which  followed  a protracted  period  of  disturbance  and  denudation 
before  the  deposition  of  the  overlying  detrital  and  iron-bearing  rocks 
of  the  region.  Taking  Major  Brooks’s  detailed  map  of  the  Menominee 
district,  published  in  the  atlas  of  the  Wisconsin  survey,  I platted  upon 
it  all  of  the  exposures  described  by  Rominger  and  not  mapped  by 
Brooks,  which  exposures  amount  in  all  to  a large  number.  Examining, 
then,  the  more  important  of  the  exposures  of  the  region,  I encountered 
still  others,  which  were  also  platted  upon  the  same  map.  Two  sections 
were  then  constructed  across  the  district  from  southwest  to  northeast, 
upon  which  wereplatted  all  of  these  exposures,  with  their  dips ; and  it 
should  be  said  that  very  many  new  facts  in  this  direction  have  been 
developed  of  late  years  by  mining. 


H U R O A FT  I -A  1ST 

iS'.W  G Sch,  /TeTcd  E D G c C D E D C D~i  D C B COED  C B ^ G 


Fig.  3.  Hypothetical  section  of  the  Menominee  region  in  the  vicinity  of  Quinnesec  Valley,  accord- 
ing to  R.  D.  Irving.  A,  basal  sericitic  quartz  slates ; B,  quartzite;  C,  limestone;  D.  iron  horizon  ; E, 
slates  and  quartzites;  G,  granite  and  Sch.,  schists  of  the  Laurentian.  Scale,  13,000 feet  to  the  inch. 


It  has  thus  become  evident  that  a structure  such  as  is  indicated  in 
the  accompanying  Fig.  3 would  not  only  coincide  with  the  recorded 
facts  as  well  as  the  sections  of  Brooks  above  given,  but  very  much  bet- 
ter than  those. 

made  ■without  the  study  of  thin  sections  hf  the  slaty  rocks  here  exposed.  When  examined  microscopi- 
cally, these  rocks  show  their  completely  fragmental  nature,  all  the  alteration  that  they  have  under- 
gone having  been  in  the  nature  of  a metasomatic  development  of  mica  flakes.  Both  hand  specimens 
and  thin  sections  of  these  slates,  moreover,  show  a most  striking  similarity  between  them  and  the 
slaty  rocks  which  frequently  lie  at  the  base  of  the  Penokee  series  of  northern  Wisconsin  and  Michi- 
gan, where  they  are  often  in  contact  with  granitic  rocks,  of  which  they  hold  fragments.  Similar  slates 
are  met  with  in  a number  of  places  at  the  base  ox  the  iron-bearing  series  of  the  Marquette  region.  As 
seen  at  the  Sturgeon  Falls,  these  slates  are  at  times  fine  grained  and  thinly  laminated,  arenaceous  and 
sericitic,  and  again  more  closely  grained  and  of  a vitreous  quartzitic  appearance,  in  which  cases  the 
predominating  quartz  fragments  have  been  cemented  together  by  secondary  enlargement.  Their  entire 
ackof  anything  like  metamorphism  is  perfectly  plain,  even  without  the  examination  of  the  thin  sec- 
tion, to  any  one  who  has  studied  many  sections  of  such  rocks  from  the  Lake  Superior  country.  The 
pebbles  in  these  slates  are  arranged  in  bands,  with  intervening  less  pebbly  or  non-pebbly  portions, 
which  portions  are  the  ones  which  show  particularly  the  ripple-marked  surfaces.  The  pebbles  are  in 
the  main  of  a pinkish  granite  and  gneiss,  wholly  identical  with  the  mass  of  granite  and  gneiss  against 
which  they  lie,  but  include  also  a smaller  number  of  pieces  of  white  quart  z and  of  a fine-grained  green- 
stone or  greenstone  schist.  Entirely  similar  quartz  occurs  in  seams  in  the  granite  close  by,  as  do  also 
masses  of  greenstone  and  greenstone  schist.  Net  only  these  pebbles,  but  the  whole  make-up  of  the 
finer  portion  of  the  rock,  make  it  entirely  evident  to  me  that  we  have  here  to  do  with  a detritus  derived 
by  water  action  from  the  granitic  and  gneissic  area  immediately  to  the  north.  The  slight  inclination 
away  from  the  vertical  towards  the  granite  which  these  conglomeratic  slates  sometimes  show  is,  of 
course,  no  argument  against  their  having  been  deposited  upon  that  granite  as  a substratum. 


THE  GREENSTONE  SCHIST  AREAS  OF  THE  MENOMINEE  AND 
MARQUETTE  DISTRICTS,  MICHIGAN. 


By  George  Huntington  Williams. 


INTRODUCTION. 

This  memoir  is  intended  as  a contribution  to  the  subject  of  dynamic 
or  regional  metamorphism.  It  contains  the  results  of  a careful  study, 
both  in  the  field  and  in  the  laboratory,  of  an  extensive  series  of  erup- 
tive rocks,  for  the  most  part  of  basic  character.  Although  the  original 
character  of  these  rocks  is  still  evident,  they  are  to  a large  extent 
cleavable,  and  the  production  of  this  secondary  feature  has  been 
accompanied  by  more  or  less  extensive  chemical  and  structural  altera- 
tions. 

It  is  the  aim  of  this  paper  to  trace  each  of  the  rock  types  repre- 
sented within  the  areas  studied  from  its  least  altered  to  its  most 
altered  form,  and  to  discuss  what  may  have  been  the  agencies  which 
produced  the  changes  noticed. 

The  rocks  selected  as  likely  to  throw  additional  light  upon  the  meta- 
morphism  of  eruptive  masses  are  so-called  i(  greenstones  ” and  a green- 
stone schists,”  which,  in  association  with  certain  more  acid  types,  cover 
extensive  districts  on  the  south  shore  of  Lake  Superior,  where  they 
lie  immediately  beneath  the  iron-bearing  strata.  Two  distinct  and 
sharply  defined  areas  of  these  rocks  were  choseu  as  typical  of  the 
whole  formation.  Particulars  regarding  their  geographical  positions 
and  their  geological  relationships  have  already  been  given  by  Professor 
Irving  in  his  preliminary  note.  In  the  first  area,  situated  on  the 
Menominee  River,  the  eruptive  character  of*  the  greenstones  and  green- 
stone schists  is  plainly  evident ; within  the  second  area,  near  the  city 
of  Marquette,  the  original  character  of  the  rocks  is  much  less  apparent. 

The  investigations,  the  results  of  which  are  embodied  in  this  mem- 
oir, were  first  suggested  to  me  in  the  spring  of  1885  by  the  late  Prof. 
R.  I).  Irving,  while  he  was  in  charge  of  the  Lake  Superior  division  of 
the  U.  S.  Geological  Survey.  Their  aim  was  to  discover,  if  possible, 
the  origin  of  the  greenstone  schists  of  the  Lake  Superior  region,  and 
at  the  same  time  to  afford  a contribution  to  our  knowledge  of  the  meta- 
morphism of  basic  eruptive  rocks  in  general.  In  the  latter  sense  they 
form  a continuation  of  the  writer’s  earlier  studies  of  the  less  altered 
gabbros  occurring  near  Baltimore,  Maryland.1 


1 Bull.  U.  S.  Geol.  Survey,  No.  28,  1886, 


31 


32 


GREENSTONE  SCHIST  AREAS  OF  MICHIGAN. 


[BULL.  62. 


Three  weeks  of  the  field  season  of  1885  were  spent  in  the  Menomi- 
nee Valley,  and  four  weeks  of  1886  in  the  neighborhood  of  Marquette. 
During  this  time,  with  the  assistance  of  Prof.  W.  S.  Bayley,  the  rocks 
were  examined  in  the  field,  and  ample  material  was  collected  for  their 
laboratory  study,  which  was  carried  on  at  the  Johns  Hopkins  Uni- 
versity, Baltimore,  Maryland,  during  the  winters  of  1885-’86  and  1886- 
’87,  at  such  times  as  could  be  spared  from  regular  university  duties. 
The  entire  investigation  has  been  conducted  under  the  auspices  of 
Professor  Irving,  for  whose  uniform  kindness  and  constant  readiness  to 
supply  every  facility  for  the  work  I gladly  take  this  opportunity  of 
expressing  my  sense  of  deep  obligation.  My  thanks  are  also  due  to 
Maj.  T.  B.  Brooks  and  to  Prof.  Raphael  Pumpelley  for  the  loan  of 
microscopic  sections  of  the  Marquette  and  Menominee  rocks,  prepared 
during  the  course  of  the  Wisconsin  State  Geological  Survey ; and  to 
Mr.  Andrew  0.  Lawson,  Ph.  D.,  lately  of  the  Canadian  Geological  Sur- 
vey, for  the  opportunity  to  make  a comparative  study  of  closely  allied 
rocks  from  the  Lake  of  the  Woods  and  the  Rainy  Lake  regions. 

I feel  that  no  especial  apology  is  needed  for  the  constant  use  through- 
out this  paper  of  the  term  44  greenstone.”  An  opinion  prevails  that  this 
word  is  antiquated  and  not  consistent  with  the  scientific  accuracy  now 
obtainable.  The  very  indefiniteness  of  this  designation,  however,  con- 
stitutes its  chief  value.  It  is  essentially  a field  term,  such  as  it  is  not 
only  desirable  but  absolutely  necessary  to  employ.  It  is  often  impos- 
sible to  state  with  certainty  in  the  field  whether  a given  basic  massive 
rock  is  a gabbro,  a diabase,  or  a diorite ; indeed,  where  such  masses  have 
undergone  extensive  metamorphism,  as  in  the  regions  here  studied,  even 
the  most  careful  microscopical  and  chemical  investigation  may  prove 
inadequate  to  disclose  what  was  the  original  form.  Wherever  accurate 
diagnosis  was  possible,  correspondingly  definite  terms  have  always 
been  employed ; but  for  use  in  the  field  or  where  the  processes  of  alter- 
ation have  obscured  the  original  character  of  the  rock  beyond  recogni- 
tion, an  intentionally  indefinite  designation  is  necessary.  For  such  a 
purpose  it  is  believed  that  no  term  is  better  fitted  than  the  ancient  and 
much  abused  ‘‘greenstone.” 

For  convenient  reference  the  specimen  numbers  belonging  to  the  col- 
lections of  the  Lake  Superior  division  of  the  U.  S.  Geological  Survey 
are  here  appended. 


1.  Menominee  Valley 

Sturgeon  Falls 

Little  Quinnesec  Falls 
Big  Quinnesec  Falls. .. 

Horse  Race 

Four  Foot  Falls 

Twin  Falls 

2.  Marquette  region 

Marquette  area 

Negaunoe  area .. 


11000-11196 

11153-11174 

11000-11048;  11098-11103 
11049-11085 

11086-11096;  11182-11196 

11142-11152;  11175-11181 

11120-11141 

11610-11864 

11610-11734 

11735-11812 


Northern  area 

3.  Agglomerates  of  Deer  Lake 


11813-11864 

12023-12058 


WILLIAMS.] 


INTRODUCTION. 


33 


The  material  embodied  in  the  present  paper  will  be  arranged  in  three 
separate  divisions. 

1.  In  chapter  one  the  importance  of  the  service  which  the  microscope 
is  capable  of  rendering  toward  the  solution  of  the  questions  of  archaean 
geology  will  be  indicated  and  a summary  presented  of  the  chief  results 
already  obtained  by  various  workers  in  this  field. 

2.  In  chapters  two,  three,  four,  and  five  the  observations  collected 
during  an  extended  study  of  the  rocks  of  the  two  areas  selected  will 
be  given  in  detail. 

3.  In  chapter  six  a connected  discussion  of  these  results  will  be  at- 
tempted, and  a comparison  of  them  with  those  reached  by  other  observ- 
ers, as  enumerated  in  chapter  one,  will  be  made. 

Bull.  62 3 


CHAPTER  I. 


PRESENT  STATE  OF  OUR  KNOWLEDGE  REGARDING  THE  META- 
MORP.HISM  OF  ERUPTIVE  ROCKS. 1 

VALUE  OF  THE  MICROSCOPE  IN  THE  STUDY  OF  METAMORPHISM. 

In  comparison  with  the  results  which  have  been  obtained  during 
nearly  a century  of  patient  research  among  sedimentary  deposits, 
the  progress  thus  far  made  in  the  domain  of  archean  geology  ap- 
pears small.  Theories  of  the  origin  of  theso-called  crystalline  schists 
are  almost  as  numerous  as  the  investigators  who  have  examined  them, 
and  yet  the  more  extensive  and  critical  the  studies  of  these  rocks 
become  the  more  obscure  and  anomalous  do  they  appear.  So  varied 
are  the  facts  which  Nature  presents  to  the  observer  in  the  oldest  rocks 
of  the  planet  that  the  conviction  is  soon  reached  that  no  single  hypoth- 
esis or  explanation  can  account  for  them.  It  is  therefore  from  no  lack 
of  interest  attaching  to  the  study  of  pre-fossiliferous  rocks  that  they 
have  heretofore  yielded  so  little  fruit,  but  rather  from  the  insurmount- 
able difficulties  which  have  stood  in  the  way  of  their  satisfactory  inves- 
tigation. That  the  study  of  fossils  has  made  up  so  large  a part  of  what 
has  been  known  as  geology  is  the  result  rather  of  necessity  than  of 
choice.  The  lack  of  exact  and  delicate  methods  of  lithological  research 
has  confined  the  attention  of  investigators  to  those  formations  where 
lithological  characters  are  of  little  value  on  account  of  the  presence 
of  other  and  more  certain  guides.  The  basement  underlying  all  of  the 
fossiliferous  rocks  has,  therefore,  remained  well-nigh  a terra  incognita, 
because  there  seemed  to  be  no  available  means  of  exploring  it. 

The  recent  multiplication  of  refined  methods  for  the  investigation 
of  crystalline  rocks,  however,  has  opened  an  almost  new  field  of  geo- 
logical inquiry.  The  difficult  and  obscure  problems  here  presented 
may  now  be  attacked  by  truly  scientific  methods.  The  prophecies 
which  Hermann  Vogelsang  made  in  18672  for  the  new  departure  in 
geology  have  been  more  than  realized  within  the  last  twenty  years. 
The  almost  new  science  of  petrography  may  be  said  to  have  proved 
itself  capable  of  rendering,  in  the  study  of  the  crystalline  rocks,  a serv- 
ice equal  to  that  which  paleontology  has  already  given  in  the  de- 
ciphering and  correlating  of  the  fossiliferous  strata. 

1 This  chapter  was  written  as  it  now  stands,  excepting  an  occasional  foot  note,  in  1887. 

2 Die  Philosophic  der  Geologic,  Pt.  3,  Moderne  Geologic  oder  mikroskopischc  Gesteinsstudien. 

34 


. williams.]  DEVELOPMENT  OF  MICROSCOPICAL  PETROGRAPHY. 


35 


Petrography,  in  its  rapid  development  since  the  introduction  of  the 
microscope,  has  already  passed  through  two  distinct  periods  and  is 
now  entering  upon  a third  and  most  important  stage.  At  first  methods 
had  to  be  perfected  for  identifying  the  various  constituents  of  crystal- 
line rocks.  During  this  stage  the  science  was  purely  mineralogical, 
although  its  methods  were  necessarily  somewhat  different,  both  in  their 
nature  and  in  their  application,  from  those  of  ordinary  mineralogy.  The 
attainment  of  this  end  required  the  study  of  a vast  amount  of  material 
wholly  without  reference  to  its  geological  significance.1 

The  second  period  in  the  development  of  petrography  was  occupied 
with  the  investigation  of  practically  unaltered  rock-types,  i.  e.,  of  rocks 
in  which  the  miuerals  and  structure  produced  by  their  original  solidifi- 
cation are  still  readily  discernible.  It  has  been  found  from  such  studies 
that  the  relationship  of  the  component  minerals  to  one  another,  or  rock- 
structure,  expresses,  to  a large  degree,  the  circumstances  under  which 
the  original  solidification  took  place,  and  hence  the  importance  of  the 
second  stage  in  the  development  of  modern  petrography. 

The  most  important  problems  presented  by  an  unaltered  massive  or 
igneous  rock  relate  to  (1)  its  chemical  composition  and  (2)  to  the  con- 
ditions under  which  it  was  formed.  The  composition  expresses  itself, 
in  a general  way,  in  the  nature  of  the  component  minerals,  while  phys- 
ical conditions  attendant  upon  the  formation  of  the  rock  may  be  traced 
in  its  structure.  Each  of  these  has  therefore  been,  in  turn,  the  partic- 
ular object  aimed  at  during  the  first  two  periods  of  petrographical  re 
search. 

But  if  petrography  were  able  to  solve  satisfactorily  all  the  problems 
presented  by  the  unaltered  massive  rocks,  it  would  even  then  be  pre- 
pared only  to  commence  its  most  difficult  and  most  important  mission. 
Rocks  are  in  reality  far  from  being  the  dead,  inert,  stationary  masses 
which  they  appear  to  the  ordinary  observer.  The  fascinating  study  of 
chemical  geology,  especially  when  aided  by  the  microscope,  shows  them 
to  be  in  a state  of  almost  constant  change.  It  is  true  that  some  of  the 
oldest  rocks  seem  to  have  suffered  hardly  any  alteration  since  they 
were  first  formed,  but  most  of  them  are  ever  active  laboratories  where 
old  products  are  being  pulled  to  pieces  and  new  ones  built  up.  The 
tracing  out  cf  such  changes  is  an  important  aim  of  petrography  in  its 
present  stage. 

The  student  at  the  microscope  wonders  at  the  minute  bubbles  which 
he  so  often  finds  inclosed  in  the  little  cavities  in  quartz.  So  delicately 
are  they  poised  that  they  are  sensitive  to  all  the  slight  oscillations  of 
temperature  that  constantly  pass  through  the  microscopic  section,  and 
the  little  prisoners  keep  up  a never-ending  movement,  as  though  beat- 

’Tlio  writer  lias  given  an  account  of  the  development  of  these  methods  in  a small  pamphlet,  entitled 
“Modern  Petrography,”  published  as  No.  1 of  the  Monographs  of  Education,  by  Heath  & Co.,  of 

Boston. 


36 


GREENSTONE  SCHIST  AREAS  OF  MICHIGAN. 


[BULU  62. 


ing  against  every  side  of  their  narrow  cell  in  the  vain  search  for  an 
exit.  Scarcely  less  delicate  seems  to  be  the  equipoise  between  the  va- 
rious chemical  compounds  in  the  earth’s  crust  and  the  surrounding 
physical  conditions  under  which  they  exist.  Like  the  constant  changes 
of  temperature  which  pass  through  the  slide  are  the  changes  in  physi- 
cal conditions  to  which  a rock-mass  is  subjected.  With  these  comes  a 
state  of  more  or  less  unstable  equilibrium  to  the  chemical  compounds, 
and,  like  the  vibrations  of  the  bubble,  molecular  movements  and  re- 
arrangements result. 

There  are  two  distinct  kinds  of  alteration  which  take  place  in  a solid 
rock-mass,  dependent,  of  course,  on  the  nature  of  the  changed  physical 
conditions.  These  are : , - 

(1)  Metamorphism  ; or  the  passage,  under  circumstances  of  high  tem- 
perature or  pressure,  or  both,  of  less  crystalline  into  more  crystalline 
compounds;  or  the  change  of  minerals  into  others,  not  less  crystalline 
or  insoluble  than  themselves. 

(2)  Decomposition  or  weathering ; the  passage,  under  ordinary  at- 
mospheric conditions,  of  crystalline  rock  constituents  into  compounds 
less  crystalline  and  more  soluble  than  themselves.  This  is  accomplished 
generally  by  hydration  or  carbonatization. 

Both  of  these  processes  are  frequently  seen  to  have  gone  on  in  suc- 
cession in  the  same  rock-mass,  the  latter  more  or  less  completely  ef- 
facing the  effects  of  the  former.  While  distinct,  both  processes  agree 
in  being  atomic  and  molecular  rearrangements  in  a solid  mass,  necessi- 
tated by  some  change  in  external  conditions.  The  differences  in  these 
conditions,  however,  produce  widely  different  results;  and  all  of  these 
again  are  essentially  different  from  those  produced  by  the  solidification 
of  a liquid  magma. 

The  student  of  the  crystalline  rocks  can  distinguish  in  a general 
way  four  classes  of  constituent  minerals,  and  this  is  true  in  spite 
of  the  fact  that  the  same  species  may  be  represented  in  two  or  more  of 
these  classes. 

(1)  Original  minerals  of  the  acid  rocks,  formed  by  solidification  of  a 
magma  in  a state  of  aqueo-igneous  fusion  or  by  the  aid  of  mineral- 
izers ; e.  g.,  quartz,  orthoclase,  mica,  zircon,  etc. 

(2)  Original  minerals  of  the  basic  rocks,  formed  from  a state  of  dry 
fusion;  e.  g.,  plagioclase,  augite,  olivine,  etc. 

(3)  Metamorphic  minerals,  formed,  as  above  explained,  from  original 
minerals;  e.  g.,  hornblende,  albite,  biotite,  zoisite,  garnet,  staurolite, 
andalusite,  etc. 

(4)  Decomposition  minerals ; e.  g.,  chlorite,  quartz,  carbonates,  the 
hydroxides,  etc. 

Such  a division,  though  necessarily  not  a sharp  one,  is  still  not 
unwarranted  and  shows  how  it  is  possible,  with  the  aid  of  the  micro- 
scope, not  merely  to  study  the  composition  of  a rock  in  its  component 
minerals,  or  the  conditions  under  which  it  was  first  formed  in  its 


Williams.1  CONTACT  AND  REGIONAL  METAMORRHISM.  3? 

structure,  but  also  to  trace  out  life  histories.  We  may  discover  not 
only  the  conditions  under  which  a rock-mass  solidified,  but  we  may 
learn  as  well  something  of  all  the  conditions  to  which  it  has  subse- 
quently been  subjected. 

Metamorphism,  or  the  recrystallization  of  rocks,  whether  massive  or 
stratified,  igneous  or  sedimentary,  is  as  varied  in  its  results  as  the 
materials  acted  upon  aud  the  agencies  which  produce  it.  How  true 
this  is  may  be  seen  where  the  cause  of  the  change  is  local  and  well 
understood,  as  in  the  numerous  instances  of  contact-metamorphism 
which  have  been  studied  in  detail  during  the  last  fifteen  years.  Here 
the  alteration  produced  by  the  same  eruptive  mass  is  different  in 
a shale  from  that  in  a sandstone,  and  in  each  the  alteration  is  quite 
distinct  from  that  produced  in  a limestone.  If  intrusive  rocks  fall 
withiu  the  range  of  influence,  the  effects  produced  in  them  are  again 
different;  while  still  wider  variations  are  noticeable  if  the  character  of 
the  active  or  metamorphosing  rock  be  changed.  This  may  be  seen  in 
the  contrast  between  the  effect  produced  by  a mass  of  granite  and  a 
mass  of  diabase  upon  the  same  surrounding  rock.  Still  other  differ- 
ences are  traceable  to  the  probable  action  of  vapors,  as  in  the  case  of 
a local  development  of  tourmaline  or  topaz  within  the  limits  of  a granite 
contact  zone. 

How  much  greater  then  might  we  expect  the  differences  to  be  which 
all  the  complicated  and  imperfectly  understood  conditions  of  regional 
metaraorphism  produce.  Many  rocks  occupying  large  areas  exhibit  a 
character  very  similar  to  that  of  rocks  which  have  been  produced  by 
contact-metamorphism,  without  there  being  any  cause  to  which  the 
alteration  can  be  so  directly  attributed.  In  some  schists,  like  those  of 
the  Ardennes  Mountains 1 and  those  of  Bergen  in  Norway,2  and  in 
many  limestones,  metamorphic  minerals  have  been  extensively  devel- 
oped without  the  total  obliteration  of  organic  remains.  In  the  case 
of  other  rocks,  of  essentially  the  same  character  though  perhaps  more 
crystalline,  the  internal  evidence  or  the  stratigraphical  relations  are 
enough  to  prove  that  they  are  metamorphosed  sediments. 

Many  of  the  so  called  crystalline  schists  present  features  of  both 
composition  and  structure  which  are  strikingly  similar  to  those  of 
rocks  of  undoubted  metamorphic  origin,  but  nevertheless  we  have  at 
present  but  few  data  for  constructing  a satisfactory  explanation  of  the 
origin  of  these  enigmatical  formations,  Theorizing  in  regard  to  them 
has  done  its  best,  and  has  succeeded  in  introducing  only  confusion  and 
disagreement.  As  before  remarked,  the  variety  here  is  far  too  great  to 
be  accounted  for  by  a single  hypothesis,  however  broad.  Many  agencies 
have  been  at  work,  whose  exact  nature  and  importance  only  the  most 
laborious  and  patient  investigation  can  show.  In  working  in  Archean 

*A.  Reward:  Lea  roclias  grenatif&res  ct  arapliiboliques  de  la  region  do  Bastogno.  Bull.  Mua.  Roy. 
Hist.  Nat.  Belgique,  1882,  vol.  i,  pp.  1-54. 

* H.  II.  Renach : Silurfoaailer  og  prcaaedo  Konglom crater  i Borgonsakifrone,  1882.  Germ,  tranal.  by 

by  R.  Baldauf. 


38 


GREENSTONE  SCHIST  AREAS  OF  MICHIGAN. 


[BULL.  62. 


geology  the  only  safe  method  is  to  free  the  mind  completely  from  all 
traditions  and  theories — to  start  with  the  idea  that  almost  nothing  is 
known  with  certainty  and  that  everything  is  to  be  discovered.  The 
facts  must  be  most  critically  observed  and  considered,  without  too  great 
a tendency  to  use  them  at  once  for  the  deduction  of  general  principles. 
Only  such  conclusions  as  can  not  be  doubted  by  any  one  who  will  take 
the  pains  to  examine  the  facts  are  of  real  value  to  the  advance  of  arch- 
ean  geology;  and  every  careful  student  in  the  field  must  realize  how 
slow  and  difficult  such  an  advance  must  be.  Detailed  analyses  of  the 
workings  of  some  well  recognized  agency,  made  where  the  action  has 
been  as  little  as  possible  disguised  and  complicated  by  the  action  of 
other  agencies,  must  yield  valuable  assistance  in  the  penetration  of  the 
mysteries  which  now  everywhere  surround  the  prefossiliferous  forma- 
tions of  the  earth’s  crust.  Such  work  has  been  done  in  Europe  and  has 
been  begun  in  America.  The  little  that  has  already  been  accomplished 
in  this  manner  is  full  of  promise  for  the  future.  The  most  striking  ex- 
ample of  work  of  this  kind  is  perhaps  that  of  Lossen  in  the  Hartz 
Mountains,  and  it  is  with  the  sincerest  appreciation  of  his  method  and 
results  that  the  present  studies  have  been  prosecuted. 

If  it  be  granted,  as  it  must  be,  by  every  impartial  observer  that  such 
a thing  as  regional  metamorphism  does  exist — that  certain  rocks,  wheu 
they  are  subjected  to  enormous  strains,  and  are  upheaved,  crushed,  and 
crumpled  do  become  more  crystalline  or  have  their  crystallization  al- 
tered—then  we  have  a well  recognized  agency  whose  particular  results 
are  worthy  of  patient  and  detailed  study.  What  part  regional  meta- 
morphism has  had  in  the  production  of  the  archean  rocks  as  a whole, 
future  years  must  show.  This  question  lies  wholly  without  my  present 
purpose;  and  yet  it  is  hoped  that  an  extended  investigation  of  a par- 
ticular phase  of  it  may  aid  in  the  final  solution  of  the  problem. 

The  investigation  was  undertaken  with  a firm  conviction  of  the  pe- 
culiar advantages  offered  by  eruptive  rocks  for  the  accurate  tracing  of 
progressive  metamorphism,  an  advantage  which  Prof.  A.  K.  Lossen 
seems  to  have  been  the  first  to  emphasize,  if  we  may  judge  from  the 
following  extract  from  one  of  his  papers.  He  says : 1 

I attribute  the  extreme  value  of  such  metamorphosed  eruptive  rocks  for  the  general 
theory  of  metamorphism  to  the  fact  that  they  are  certainly  known  to  have  been  de- 
rived from  a solid  rock  of  definite  mineral  aggregation,  average  chemical  composition 
and  structure.  In  the  primary  minerals  and  structures  of  the  igneous  rocks  we  pos- 
sess a well  known  quantity,  upon  which  we  can  base  our  conclusions — a definite  scale 
according  to  which  the  nature  and  amount  of  those  secondary  minerals  and 
structures  characterizing  the  metamorphic  rocks  can  he  measured.  Frequently 
the  certain,  incontestable  fact  of  pseudomorphism  proves  the  secondary  alteration  of 
these  rocks  in  a much  more  general  way  than  even  the  very  exceptionally  preserved 
fossil  remains  are  able  to  prove  the  origin  of  metamorphosed  sediments.  , 

1 Den  hohen  Wertk  dieser  metamorpbiacben  Eruptivgesteino  fur  die  Lelire  voni  Metamorpbismus 
fand  icb  darin,  dass  ein  von  Ilaus  aus  festes  Gestein  vonganz  bestimmter  Mincralaggregation,  chemischer 
Durchschnittszusammemetzung  tend  Structur,  zuverlassig  als  ibr  Muttergestein  angegebeu  werden 
kann.  In  den  priiniiren  Mineralicn  und  primaien  Structurpn  der  Erstarrungsgesteine  besitzcn  wir  eine 


WILLIAMS.] 


CHANGES  IN  ROCK-FORMING  MINERALS. 


39 


There  is  no  student  of  mineralogy  who  has  not  been  struck  with  the 
great  similarity  which  exists  in  the  composition  of  so  many  of  the 
rock-forming  silicates. 

We  have  after  all  a very  small  number  of  bases  in  these  silicates  and 
they  are  often  combined  in  almost  the  same  proportion  in  minerals 
which  show  the  greatest  disparity  of  crystal  form,  physical  properties, 
and  mode  of  occurrence.  It  seems  to  be  oftentimes  more  a matter  of 
external  condition  rather  than  of  chemical  composition,  which  deter- 
mines what  particular  mineral  is  formed ; and  the  equipoise  between 
the  existence  of  a certain  silicate  and  the  external  conditions  is  often 
so  delicate  that  a mere  change  in  the  latter  is  alone  sufficient  to  de- 
stroy the  mineral  as  such  and  to  cause  it  to  change  to  some  other  mod- 
ification or  compound.  The  recent  discoveries  of  the  alterations  which 
dimorphous  bodies,  like  leucite  or  tridymite  undergo,  show  how  this 
may  be  accomplished  without  chemical  change.  The  breaking  up  of  a 
mineral  into  an  aggregate  of  two  or  more  is  not  less  common ; as  for 
example,  the  passage  of  piagioclase  iuto  zoisite  and  albite  (saussiirite), 
or  of  spodumene  into  albite  and  eucryptite  (the  /?-spodumene  of 
Brush  and  Dana.)1  This  subject  has  lately  been  elaborated  by  Prof. 
J.  W.  Judd  in  his  presidential  address  before  the  Geological  Society  of 
London,  and  in  many  others  of  his  recent  papers.2 

Bocks  whose  component  minerals  are  so  delicately  balanced  to  accord 
with  the  particular  set  of  conditions  under  which  they  were  formed, 
must  be  peculiarly  subject  to  alteration  when  these  conditions  are 
changed  j and  for  this  reason  the  writer  lias  before  insisted  that  erup- 
tive rocks  must  be  even  more  liable  to  metamorphism  than  the  sedi- 
ments which  contain  them.3 

The  advantage,  then,  of  eruptive  rocks,  especially  of  basic  eruptive 
rocks,  for  the  study  of  metamorphic  processes  is,  as  Lossen  has  remarked 
with  so  much  force,  because  we  have  in  them  a set  of  minerals  and 
structures  which  can  with  certaiuty  be  referred  to  eruptive  conditions, 
i.  e.,  conditions  of  fusion.  These,  at  least  for  the  basic  rocks,  may  be 
easily  reproduced  in  the  laboratory,  as  has  been  so  successfully  done  by 

wohlbokannte  Grosse,  die  wir  unserem  Urtheil  zu  Grande  legen  konnen,  einon  festen  Maassstab,  ail 
welchem  Art  und  Grad  jener  secundaren  Mineralien  und  socundareu  Structure!*  gemessen  werdenkbn- 
nen  welche  die  Natur  des  metamorphischen  Gesteins  melir  oder  weniger  auamacbon.  Vielfacb  ist  es 
geradezu  diesichero,  uuanfechtbare  Thatsache  der  Pseudomorphosenbilduug,  die  in  solchen  Gestoinon 
jn  viel  allgemeinerer  Weise  bewcisend  fur  die  Umbildung  eintritt,  ala  dio  nur  unter  besonders  guns- 
tigen  Umstanden  erhalteuon  Petrafacton  in  den  metamorpliisirten  Sedimenten.  Jahrbuck  dor  kbnig- 
lichen  preussischen  geologiscben  Landesanstalt  u.  Bergakademie  fiir  1883,  Berlin,  1884,  p.  G20. 

On  page  619  ibid.,  Lossen  in  a note  gives  the  foll(>wing  list  of  references  to  his  former  remarks  on  this 
same  important  topic:  Zeitsclirift  der  deutschon  gcologischen  Gosollscbaft,  vol.  21,  p.  298,  1869;  vol. 
24,  pp.  706,  707,763,  1872;  vol.  27,  pp.  451  and  969,  1875;  vol.  29,  p.  360,  1877;  Sitzungsbericlito  der  Go- 
sellscliaft  naturforschender  Freunde  in  Berlin,  Mch.,  1878;  Jan.,  1880,  and  Nov.,  1883;  Jahrlmchder 
kbngl.  preuss.  geologiscben  Landesanstalt  fiir  1880,  p,  12;  fiir  1881,  p.  43,  and  finally  in  the  Erliiute- 
rungen  zur  geologiscben  Specialkarte  von  Prcussen  und  don  thiiriugisekon  Staaton.  Blatter:  llarz- 
gorodo  (p.  79)  ; Wippra  (pp.  27,  43) ; Sohwenda  (p.  34). 

1 Am.  Jour.  Sci.,  3d  sor.,  vol.  20,  1880,  p.  257,  and  Zoitschr.  Kryst.  u.  Minoral.,  vol.  5,  p.  192. 

2Quar.  Jonr.  Geol.  Soc.  London,  vol.  43,  1887.  Proc.  pp.  54-82. 

3 Boll.  U.  S.  Geol.  Survey,  No.  28,  p.  9,  10. 


40  GREENSTONE  SCHIST  AREAS  OF  MICHIGAN.  [bull.  62. 

Messrs.  Fouque  and  Michel -L6vy,  of  Paris.1  The  exact  mineral  associa- 
tion and  structure  of  diabase  and  other  basic  igneous  rocks  may  be  syn- 
thetically reproduced  by  simple  dry  fusion,  and  there  is  no  indication 
whatever  that  they  are  ever  produced  in  nature  by  any  other  means. 
The  finding  therefore  of  such  characteristic  structure,  even  where  they 
have  been  more  or  less  disguised  by  subsequent  changes,  at  once  fur- 
nishes a definite  and  certain  starting  point.  We  know  what  the  orig 
inal  character  of  the  rocks  in  question  was  and  the  conditions  under 
which  it  was  formed;  and  the  careful  minute  study  of  the  changes 
which  the  original  component  minerals  have  undergone,  when  taken  in 
connection  with  the  external  physical  conditions  to  which  the  rock  mass 
has  been  subjected,  can  but  yield  useful  results  to  geological  science. 

HISTORICAL  OUTLINE  OF  STUDIES  ON  THE  METAMORPHISM  OF  ERUP- 
TIVE ROCKS. 

Notwithstanding  the  great  importance  which  has  always  attached  to 
the  idea  of  metamorphism,  it  is  only  within  recent  years  that  it  seems 
to  have  been  regarded  as  applicable  to  any  but  sedimentary  rocks. 
With  Hutton,  who  may  practically  be  considered  the  originator  of  the 
idea,  and  with  Lyell,  to  whom  we  owe  the  term  which  describes  it,  met- 
amorphism was  the  gradual  consolidation , by  means  of  the  earWs  internal 
heat , of  sunJcen  and  buried  strata , whose  original  parallel  structure  was 
not  wholly  obliterated  by  the  change.  So  strong  has  the  power  of  this 
tradition  become,  that  it  is  not  easy  to  overcome  it  even  at  the  present 
time.  Nor  after  the  discovery  and  satisfactory  explanation  of  second- 
ary (slaty)  cleavage  in  rock-masses,  was  the  case  much  better.  The 
distinction  between  foliation  and  stratification  was  accepted  as  rad- 
ical, and  it  was  generally  conceded  that  the  former  was  secondarily 
developed  in  solid  masses  as  the  effect  of  pressure,  and  yet  we  hear  of  it 
chiefly  in  sedimentary  rocks — in  slates  and  shales.  The  eruptive  rocks 
seem  to  have  been  regarded  as  too  hard  and  unchangeable  to  be  affected 
even  by  the  enormous  forces  which  upheaved  a mountain  chain.  How 
untrue  this  is  we  are  daily  learning  from  the  study  of  rocks  undoubtedly 
eruptive,  which  possess  a pronounced  schistose  structure. 

As  we  now  look  back  over  a century  of  discussion  and  investigation 
of  metamorphism,  the  total  neglect  of  eruptive  masses,  save  as  an  active 
agent  in  the  change,  seems  surprising.  Daubree,  in  his  admirable  essay 
on  the  subject,2  has  much  to  say  of  change  of  structure,  and  yet  he 
makes  no  allusion  to  eruptive  rocks  as  being  subjected  to  it.  Delesse, 
in  the  second  portion  of  his  u Studies  of  Metamorphism”3  which  treats 
of  regional  or  normal  metamorphism,  devotes  considerable  space  to  the 
metamorphism  of  eruptive  rocks,  but  his  conclusions  are  not  such  as 
at  the  present  time  deserve  attention.  He  maintains  that  by  some 

1 Synthase  ties  mindraux  et  de  roches,  Paris,  1879. 

3 Etudes  et  exp6riences  synth6tiques  sur  le  m6tamorphi9me,  etc.,  M6ra.  presents  par  savants  \ 
l’AcadSmie  des  sciences,  vol.  17,  1862.  Translated  in  the  Smithsonian  Annual  Report  for  1861,  pp.  228-304. 

*Etudes  sur  lemGtamorphisme  des  roches.  Ouvrage  couronnG  par  l’Acad6mie  des  sciences.  Paris, 
1869. 


WILLIAMS.] 


METAMORPHISM  OF  ERUPTIVE  ROCKS. 


41 


vague  process  of  “general  metauiorphism  ” volcanic  rocks  are  changed 
to  plutonic.  Thus  a trachyte  becomes  a granite  ; aucl  a trap,  a diorite. 
The  absence  of  volcanic  rocks  in  the  oldest  formations  is  accounted  for 
by  the  great  length  of  time  during  which  these  have  been  subjected  to 
metamorphosing  agencies.  The  original  plutonic  rocks  are  considered 
to  be  capable  of  little  or  no  change. 

One  of  the  first  truly  scientific  studies  of  the  metamorphism  of  erup- 
tive rocks,  based  purely  on  careful  observation  of  the  facts,  was  that  of 
Lossen  in  the  Hartz  Mountains.  Here  it  was  possible  to  trace  the  nu- 
merous diabase  dikes  and  larger  areas  of  more  coarsely  crystalline  gab- 
bros,  along  with  the  schists  in  which  they  were  inclosed,  from  their 
unaltered  to  their  most  highly  altered  form.  Ag  early  as  1872  he  wrote 
as  follows: 

I shall  begin  with  igneous  rocks  which  have  been  altered  in  situ  and  with  their 
(final)  change  into  crystalline  schists.  The  fact  that  massive  rocks,  which  frequently 
possess  a parallel  structure  as  an  original  feature,  may,  by  metamorpliic  processes, 
be  converted  into  foliated,  but  not  on  that  account  stratified,  beds  is  incontestable.  In 
this  manner  granular  diabase  is  converted  into  leuticularly  foliated  (fiaserig)  by  the 
more  or  less  complete  passage  of  the  cleavable  augite  into  a scaly  aggregate  of 
chloritie  minerals.  The  rock  thus  assumes  a kind  of  schistose  structure,  as  is  often 
the  case  in  the  southwestern  Hartz.1 

The  cause  of  the  metamorphism,  too,  can  be  seen  in  some  cases  to 
be  the  eruption  of  large  granite  masses ; in  others,  the  orographic  forces^ 
which  had  crumpled  and  upheaved  the  entire  district.  Upon  this  subject 
Lossen  says: 

1 have  often  emphasized  the  significance  of  those  metamorphic  regions  in  which 
ernptive  rocks— interbedded  in  the  schists  and  like  them  jmssively  subjected  to  dis- 
location and  mountain-makiug  forces — have  undergone  about  the  same  substantial 
and  structural  alterations  as  the  inclosing  schists  ; nor  is  it  material  whether  this  re- 
sult has  been  accomplished  within  the  coutactTZone  of  some  intrusive  granitic  mass 
or  by  dynamic  (dislocation)  forces  properly  so  called.2 

Massive  rocks  may  therefore  be  passively  subjected  to  the  influence 
of  either  contact  or  regional  metamorphism. 

Instances  of  the  former  seem  never  to  have  received  their  merited 
share  of  attention,  and  yet  they  have  been  mentioned  in  many  different 
regions.  Allport  described  dolerites  which  had  been  altered  by  adja- 
cent eruptive  granites  in  Cornwall.3  I11  France  Michel-Levy  has  found 

‘lull  begiune  mit  den  in  situ  nnagewandelten  Erstarrungsgesteinen  und  deren  TTuawandlung  zu 
krystallinischeu  Scbiefern.  Die  Thatsache,  dass  durch  metamorphische  Proces.se  inassigo  Gesteine, 
die  haufig  bereits  cine  urspriiuglicke  plane  Parallel structur  besitzen,  in  schioliige,  darum  aber  noch 
nicht  in geschichtete,  umgewaudelt  werden,  ist  unbestreitbar.  So  geben  die  kbrnigen  Diabase  dadurch 
hiiuUg  in  flaserige  Uber,  dass  das  blatterig  brechende  augitischo  Mineral  ganz  oder  theilweiso  in  oin 
scbnppiges  Aggregat  eines  chloritischen  Minerals  urngewandelt  wird,  wobei  das  Gestein  eino  Art 
echiofrige  Structur  anuobmen  kann,  wio  dies  iin  S'udost  Harz  nicht  sclton  dor  Fall  ist.  (Zoitschr. 
Dcutsch.  gcol.  Gesell.,  Berlin,  vol.  24,  p.  763,  1872.) 

2 Merfacb  bercits  babe  ich  die  Bedeutung  solcher  metanaorphischer  Gebieto  hervorgelioben  in  welchen 
zwischcn  den  Schichten  eingoscbalteto  und  nur  passiv  ana  Faltungs-  und  Gobirgsbildnngsprocosse  bo- 
tboiligto  Ei  uptivgesteine  in  anniihernd  demsolbon  Grade  wie  die  danobon  anstehendon  Schichtgestoine 
substantiello  nnd  strecturello  Umwandlungon,  sei  es  in  der  Contactspkiire  der  in  die  Faltuug  oingrei- 
fenden  eugranitischen  Eruptivnaassen,  sei  es  durch  den  Dislocationsprocess  seb  loch  thin,  orlitten 
haben.  (Jalirb.  preuss.  gcol.  Landesaustalt  fiir  1883,  p.  G19.) 

3 On  the  metamorphic  rocks  surrounding  the  Land’s  End  mass  of  granite.  Quarterly  Journal  Geol. 
Soc.,  London,  vol.  32,  1870,  p.  422. 


42 


GREENSTONE  SCHIST  AREAS  OF  MICHIGAN. 


{BULL.  62. 


similar  effects  produced  in  the  Cambrian  diabases,1  and  Barrois' men- 
tions diorites  (u  diorite  modifie”)  which  have  been  modified  by  the  same 
cause.2  Still  more  recently  Brogger  has  discovered  the  same  class  of 
phenomena  in  dikes  of  augite  porphy rite  which  penetrate  the  strata  of 
the  classic  Silurian  region  near  Christiania.3 

The  most  exact  and  satisfactory  accounts  of  such  rocks  are,  however, 
those  given  by  Lossen  of  the  diabases  which  fall  within  the  limits  of 
the  Bamberg  granite  contact  zone  in  the  Hartz  Mountains.4  The  effect 
of  the  granite  has  been  to  produce  alterations  in  the  eruptive  diabases 
quite  analogous  to  those  usually  brought  about  by  orographic  forces. 
The  augite  has  been  changed  to  uralite,  which  surrounds  the  core  of 
the  original  mineral  in  a double  zone,  the  inner  one  being  colorless  and 
dotted  with  magnetite,  while  the  outer  one  is  composed  of  a more  com- 
pact, green,  and  pleochroic  hornblende.5  The  labradorite  of  these 
diabases  has  been  saussuritized;  their  ilmenite  has  been  changed  to 
sphene  (leucoxene)  and  their  pyrite  to  pyrrhotite.  Biotite  and  garnet 
have  also  been  occasionally  developed.  The  characteristic  diabase 
structure  is  recognizable  so  long  as  any  of  the  augite  or  labradorite 
substance  remains. 

If  the  results  described  by  Lossen  are  in  reality  wholly  due  to  the  in- 
fluence of  the  intrusive  granite  mass,  then  we  see  that  the  similarity 
between  the  effects  produced  by  contact  metamorphism  and  regional 
metamorphism  is  just  as  close  in  the  case  of  eruptive  rocks  as  it  is  in  that 
of  sedimentary  beds.  The  connection  which  exists  between  regionally 
metamorphosed  areas  and  the  disturbances  to  which  such  areas  have 
been  subjected  appears  to  be  a constant  one.  Indeed,  aside  from  the 
local  influences  of  intrusive  masses,  the  amount  of  metamorphism  may 
be  said  to  be  in  all  cases  proportional  to  the  pressure  or  strain  to  which 
the  rock  in  question  has  been  subjected.  The  recent  recognition  of  this 
fact  has  brought  into  favor  the  term  “ dynamic  metamorphismj ’6  which, 
in  a way,  expresses  the  agency  or  process  to  which  the  change  may  be 
attributed. 

Bocks  are  not  metamorphosed  by  pressure  alone,  and  yet  the  im- 
portance of  this  agency  would  appear  to  be  greater  than  that  which  has 
commonly  been  assigned  to  it.  Other  factors,  especially  heat  and 
moisture,  have  also  played  an  important  part  in  the  changes,  but  their 
efficacy  is  in  large  measure  due  to  the  direct  results  of  pressure  upon 

1 Sur  lea  roches  eruptives  basiqnes  Cambriennes  du  M&connais  et  du  Beaujolais.  Bull.  Soc.  g6ol. 
France,  3 series,  vol.  11,  1883,  pp.  273-303. 

2Lc  granite  de  Eostrenen,  ses  apophyses  et  ses  contacts.  Annales  Soc.  gdologiquo  du  Nord,  1884, 
vol.  12. 

3Spaltenverwerfungen  in  der  Gegend  Langesund-Skien.  Nyt  Mag.  for  Xaturvidenskaberne,  vol. 
23,  1884,  pp.  253-419.  . 

4 Ueber  den  Kamberg  Granit  nnd  seinen  Contact-Hof.  Erlauterungen  zu  Blatt  Harzgerode  der 

geologischen  Specialkarte  von  Preussen  und  der  thiiringiseben  Staaten.  Vide  also  Jahrb.  kdn.  preuss. 
geol.  Landesanstalt  fur  1883,  pp.  619-612  ; fur  1884,  pp.  56-112,  and  pp.  525-545. 

6 For  an  illustration  of  this  structure,  see  Bull.  U.  S.  Geol.  Survey,  No.  28,  1886,  PI.  I.  Fig.  2. 

c “Mechanical  metamorphism  ” of  Heim  audBaltzer,  “ Dislocation-M.”  of  Lossen,  “ Dynamical-M.” 
of  Eosenbusch,  “ Stauungs-M.”  of  Credner,  “ Pressure-M.”  of  Bonney. 


WILLIAMS.] 


THREE  TYPES  OF  METAMORPHISM. 


43 


the  solid  rock-mass.  The  crushing  of  rocks  along  fault  or  shearing 
planes  allows  here  of  the  ready  circulation  of  moisture  and  of  a conse- 
quent increased  distribution  of  heat.  RoeTic  are  hence  most  altered 
along  such  planes.  The  almost  universal  effect  of  such  a crushing  is 
made  apparent  by  a microscopic  examination  of  rocks  which  have  been 
subjected  to  enormous  pressure.  We  shall  have  occasion  to  cite  numer- 
ous instances  of  this  in  the  sequel.  For  the  present  we  will  state  the 
three  different  modes  in  which  an  eruptive  rock  is  altered  when  it 
undergoes  regional  or  dynamic  metamorphism,  and  mention  the  work 
of  those  who  have  been  particularly  successful  in  illustrating  the  action 
of  all  or  any  of  them. 

The  three  ways  in  which  a massive  crystalline  rock  may  be  modified 
by  the  action  of  orographic  forces  are : 

J.  Macro-structural ; i.  e.,  it  may  have  its  external  structure  (mor- 
phology) changed  so  as  to  become  schistose  or  foliated. 

II.  Micro- structural ; i.  e.,  it  may  have  its  internal  or  microscopic 
structure  (histology)  wholly  changed,  either  with  or  without  an  alter- 
ation of  the  last-mentioned  sort. 

III.  Mineralogicai ; i.  e.,  there  may  be  a change  in  the  nature  of  one 
or  more  of  the  component  minerals,  either  with  or  without  a change  in 
the  chemical  composition  of  the  rock  as  a whole. 

Of  course,  any  one  of  these  kinds  of  change  may  be  produced  in  a 
rock-mass  alone,  or  any  two,  or  even  all  three,  may  exist  simultaneously 
in  any  relative  degree  of  intensity. 

Macrostructural  Metamorphism. — It  had  already  long  been  recognized 
that  transversal  or  slaty  cleavage  could  be  produced  in  sedimentary 
beds  by  mechanical  force,1  when  A.  Heim,  in  his  work  on  the  “ Mech- 
anism of  Mountainmaking,”  published  in  1878, 2 directed  attention  to 
an  almost  new  line  of  geological  work,  by  showing  in  a very  general 
way  how  the  orographic  forces  effect  the  deformation  of  rock-masses. 
He  insisted  upon  three  main  points: 

(a)  That  the  rocks  were  solid  and  rigid  when  they  were  acted  upon. 

(b) * That  by  a moderate  pressure,  they  are  torn  asunder  and  the  thus 
formed  open  fissures  ((( klaffende  Risse”)  are  subsequently  filled  by  ma- 
terial segregated  from  the  rock  (“  adern ”).  If  the  mass  is  plastic  rather 
than  brittle,  the  strain  is  relieved  by  numerous  slicken-sides  (u  Rutsch- 
flachen”)  (“  Umformung  mit  Bruch”). 

(c)  That  by  the  most  intense  pressure  this  action  becomes  infinitely 
small  or  molecular,  i.  e.,  the  form  is  altered  without  rupture  (“  Umfor- 
mung ohne  Bruch”). 

Heim  lays  great  stress  upon  the  fact,  already  emphasized  by  Suess,3 
that  the  massive  or  crystalline  rocks  whicli  form  the  center  of  the  Al- 

1 On  slaty  cleavage  awl  allied  rock-structures  with  special  reference  to  the  mechanical  theories  of 
their  origin.  13y  Alfred  Harker.  Kept,  fifty-fifth  meeting  Brit.  Assoc.  Adv.  Sci.,  in  1885,  pp.  813-855, 

1886. 

2Untersuchnngen  liber  den  Mechanismns  dor  Gebirgsbildung  ini  Anschluss  an  die  geologische  Mono 
graphic  der  Todi-Windgallcn-Gruppe.  Basle,  1878,  Vol.  2. 

* Die  Entstehung  der  Alpen.  Wien,  1875. 


44  GREENSTONE  SCHIST  AREAS  OF  MICHIGAN.  [bull.  62. 

pine  “massivs”  were  not  themselves  in  any  way  instrumental  in  the 
elevation  of  the  mountains.  He  gives  an  elaborate  proof  that  these 
were  solid  long  before  the  elevation  ; and  were  only  passively  sub- 
jected to  the  upheaving  force,  in  the  same  way  as  the  overlying  sedi- 
ments. Heim  does  not,  however,  seem  to  apply  his  laws  of  mechanical 
deformation  to  these  crystalline  rocks,  as  he  might  well  have  done,  but 
regards  their  schistose  or  banded  structure  as  probably  an  original 
character. 

Other  geologists  were  not  long  in  recognizing  the  mechanical  defor- 
mation of  massive  as  well  as  sedimentary  rocks.  Daubree  is  struck  by 
the  frequent  gradual  passage  of  massive  rocks  into  schistose  varieties 
of  the  same  composition.  He  says  that,  in  spite  of  his  own  strong  lean- 
ings toward  the  u metamorphic  theory,”  he  can  not  possibly  regard 
such  a schistose  structure  as  any  sign  of  original  stratification  but 
must  consider  it  as  secondarily  produced  in  the  eruptive  mass  by  press- 
ure. He  is,  however,  inclined  to  believe  that  this  result  was  attained 
before  the  eruptive  rock  had  wholly  solidified.1  H.  H.  Reusch,  from 
his  studies  of  the  rocks  near  Bergen,  in  Norway,  is  also  convinced  that 
the  frequent  banding  and  gneissic  structure  in  granite  is  secondary  and 
a product  of  pressure,  like  slaty  cleavage.  Like  Daubree,  he  too  thinks 
that  it  was  accomplished  while  the  rock  was  still  somewhat  soft,  atthe 
time  of  the  faulting  and  dislocation  to  which  the  granite  owed  its  own 
elevation,  in  a plastic  state.2  This  idea  that  such  pressure  deformation 
could  only  take  place  in  softened  or  in  unsolidified  rocks  was  particu- 
larly dwelt  upon  by  Carl  Friedrich  Naumann.  How  thoroughly  the  ob- 
jections to  the  deformation  of  rigid  rock  masses,  as  far  as  sedimentary 
deposits  are  concerned,  are  answered  by  the  facts  observed  by  Heim, 
we  have  already  seen.  The  assumption  of  an  identical  process  for  the 
highly  crystalline  massive  rocks  seems,  at  first,  to  present  great  dif- 
ficulties, but  observations  in  all  parts- of  the  world  are  daily  proving 
its  necessity. 

In  1879,  Rothpletz3  showed  how  the  actinolite,  or  so-called  green- 
schists  near  Hainichen,  in  Saxony,  had  been  brecciated  by  pressure  and 
the  fragments  shoved  along  more  or  less  upon  each  other,  so  as  often 
to  produce  an  imperfect  schistose  structure.  This,  which  has  a close 
analogy  to  certain  macros tructural  modifications  of  the  Lake  Superior 
greenstones  to  be  described  in  subsequent  pages,  allowed,  as  Rothpletz 
remarked,  a much  increased  chemical  action,  which  tended  to  alter  the 
character  of  the  rock.  A.  Baltzer,  in  his  monograph  on  the  Finster- 
aarhorn,4  published  in  1880.  expresses  himself  as  decidedly  in  favor  of 
a mechanical  metamorphism  of  the  interior  crystalline  rocks.  He  says 
on  page  244  of  his  work  : 

1 iStudes  synthbtiques  de  g6ologie  exp6rimeutelle.  Paris,  1879,  p.  432. 

2Die  fossilien  fiihrenden  krystallinischen  Schiefer  von  Bergen  in  Norwegeu.  Deutsche  Aufgabe  von 
It.  Baldauf,  1883,  pp.  129,  130. 

3Uel>er  mechanisclien  Gesteinsumwandlungeu  bei  Hainichen  in  Sachsen.  II.  Die  Breccienbild- 
nng  des  Aktinolitlischiefers  von  Hainichen.  Zeitschr.  Dentsch.  geol.  Gesell,  1879,  Vol.  31,  p.  374. 

4 Die  mechanisclie  Contact  von  Gneiss  und  Kalk  iui  Berner  Oberland.  Beitrage  zur  geologischen 
Karte  der  Schweiz.  XX.  Lieferung.  Bern,  1880. 


WILLIAMS.] 


LEHMANN  ON  DYNAMIC  METAMORPHISM. 


45 


I base  my  assumption  that  the  parallelism  of  the  mica-scales  in  abnormally  strati- 
fied gneiss  is  conditioned  by  pressure,  upon  this  transverse  foliation.  Just  as  slaty- 
cleavage  is  generated  in  the  younger  sedimentary  rocks  by  pressure  and  mechanical 
deformation,  so  is  it  also  in  the  crystalline  schists.  This  may  be  proved  in  the  case 
of  the  last  named  rocks,  if  other  evidence  is  lacking,  by  its  parallelism  with  the  un- 
doubted cleavage  in  contiguous  sediments.1 

Similar  ideas  have  been  more  or  less  clearly  expressed  by  Kjerulf,  Brog- 
ger,  Stapff,  and  other  geologists,but  one  of  the  most  important  contribu- 
tions to  our  knowledge  of  this,  as  well  as  of  other  phases  of  mechani- 
cal metamorphism,  was  made  in  1884  by  Prof.  Johannes  Lehmann  in  his 
work  on  the  origin  of  the  crystalline  schists.2  That  author  has  col- 
lected an  immense  number  of  observations  from  Saxony,  Bavaria,  and 
Bohemia — especially  in  the  “ Granulite 79  district  of  the  first  named 
country,  upon  the  detailed  study  of  which  he  has  spent  many  years. 
From  these  observations  Lehmann  reaches  certain  general  conclusions 
of  importance  with  reference  to  the  mechanical  metamorphism  of  solid 
massive  rocks.  These  are  stated  in  chapters  16  and  17  of  his ‘work. 
He  regards  gneiss  as  simply  a structure  form  of  granular  feldspathic 
rocks,  and  according  to  the  composition  of  these  there  may  occur  gran- 
itic gneiss,  syenitic  gneiss,  dioritic  gneiss,  gabbro  gneiss,  etc.  He  thinks 
that  the  essential  parallel  structure  of  gneiss  may  be,  but  very  rarely 
is,  original.  He  finds  no  indication  that  any  true  gneisses  were  once 
sedimentary  deposits,  but  he  considers  them  all  as  igneous  rocks 
(“Erstarrungsgesteine”),  which,  as  a general  thing,  have  acquired  their 
present  structure  by  stretching  (“  Streckung”)  in  a solid  state.  More- 
over, gneiss  exhibits  only  the  first  stage  of  such  a mechanical  meta- 
morphism. If  the  action  of  this  process  is  more  intense,  finer  grained 
and  more  evenly  banded  rocks  result,  which  the  author  designates  as 
granulite  and  felsite  schist.  According  to  Lehmann,  therefore,  all  the 
massive  crystalline  rocks  are  subject  to  alterations  in  their  structure 
through  great  pressure  or  tension.  They  become  banded  or  schistose  in 
proportion  to  the  intensity  of  this  action. 

The  observations  of  many  workers  in  various  regions  since  the  publi- 
cation of  Lehmann’s  conclusions  have  tended  to  substantiate  them. 
Mr.  Hatch3  has  shown  the  secondary  development  of  a schistose  struct- 
ure in  the  gabbros  of  the  Tyrol,  and  the  same  thing  has  been  done  for 
the  gabbros  near  Baltimore,  Maryland.4  Besults  very  closely  resem- 
bling those  of  Lehmann  have  recently  been  secured  by  Mr.  J.  J.  H. 
Teall  in  the  gabbro  region  of  the  Lizard,  Cornwall,  England.5  This 

1 Auf  diese  transversale  Scliieferung  griinde  ich  die  Annalime  dass  dor  Paralloliruus  der  Gliminor- 
blatrchen  ira  anonnal  gelagerten  Gneiss  ebenfalls  von  Druckschieferung  herriihrt.  Wio  in  don  jiing- 
ern  Sediraentgesteincn  durch  Druck  und  niechanisclie  Umformungsprozesso  transvei  salo  Sckieferurig 
entstand,  bo  anch  in  den  krystallinisclien  Schieferu.  Bei  letzteren  kann  sie,  in  Ermangelung  andorer 
Anhaltspuukto,  durch  den  Parallelismus  mit  einor  uuzweifelliaften  Schieforuugsrichtung  in  don  au- 
grenzenden  Sediruenten  nachgewiesou  werdon. 

’Untersuchnngen  iiber  die  Entstobung  der  altkrystallinischon  Schioforgestoine,  etc.,  with  Atlas  of 
photographs.  4°.  Bonn,  1884. 

*T«ohermak’s  mineral,  ti.  petrog.  Mittheil.,  vol.  7 (1885),  p.  75. 

4 Bull.  U.  S.  Geol.  Survey,  No.  28. 

•Geol.  Mag.,  London,  November,  1886. 


46  GREENSTONE  #SCHIST  AREAS  OF  MICHIGAN.  [bull.  62. 

investigator  derives  proof  that  the  alteration  ip  structure  was  accom- 
plished after  complete  solidification  from  the  relation  of  the  rock  to 
fault-planes.  He  says: 

A rock  must  necessarily  be  solid  before  it  can  be  faulted.  Now,  we  find  at  Pen 
Voose  near  Landewednack,  that  massive  gabbro  passes  over  into  gabbro  schist  at  a 
fault-plane,  and  that  the  foliation  in  the  gabbro  is  such  as  would  be  produced  by  a 
shearing  motion  parallel  with  the  fault-plane.  Taking  all  the  facts  into  considera- 
tion, we  appear  to  be  justified  in  concluding  that  the  foliation  in  the  Lizard  gabbros 
is  the  result  of  pressure  or  regional  metamorphism. 

O.  Schmidt  has  also  recently  given  us  the  results  of  his  studies  of 
certain  eruptive  porphyries  in  the  central  Alps,  especially  in  the  Wind- 
gallen  group,  the  district  particularly  studied  by  Heim.1  These,  like 
the  surrounding  sediments,  have  been  subjected  to  euormous  pressure 
and  strains  and  thereby  have  had  developed  in  them  a pronounced 
schistose  structure,  becoming  in  some  instances  veritable  felsite  schists. 
Still  more  recently  H.  H.  Reusch  has  communicated  his  observations 
in  the  regionally  metamorphosed  district  of  Hardangerfjmxl,  on  the 
west  coast  or  Norway.2  Here  he  finds  dikes  of  all  sorts  of  eruptive 
rocks,  both  acid  and  basic,  all  rendered  secondarily  schistose  parallel 
to  the  planes  of  the  inclosing  schists,  without  reference  to  the  direction 
of  the  dikes  themselves.  This,  therefore,  can  not  possibly  be  due  to 
either  flow  or  cooling,  but  must  be  the  result  of  pressure.  Oh.  E. 
Weiss  observed  the  same  thing  in  the  quartz  porphyry  dikes  of  Thai,  in 
Thuringia.3 

Prof.  T.  G.  Bonney,  in  his  annual  presidential  address  to  the  Geo- 
logical Society  of  London  (February,  1886),  deals  with  the  subject  of 
metamorphism  in  general,  and  has  much  to  say  about  the  structural 
changes  induced  in  hoiocrystalliue  massive  rocks  by  pressure4.  He 
distinguises  between  u stratification- foliation”  and  u clear  age-foliation  fi 
the  latter  being  always  secondarily  produced  by  pressure.5  This  same 
cause  also  in  some  cases  may  produce  a false  bedding  parallel  to  the 
cleavage-foliation,  almost  exactly  similar  to  the  bedding  of  sedimentary 
rocks,  although  of  a totally  different  origin,  and  to  this  he  applies  the 
name  u pseudostromatism.”6 

Microstructural  metamorphism. — The  statement  of  Heim  that  under 
sufficient  pressure  rock-masses  became  plastic,  i.  e.,  that  they  could  be 
bent  and  crumpled  by  a true  molecular  movement  within  the  mass,  with- 
out rupture,  seems  to  have  been  based  entirely  on  a macroscopical  study 
of  exposures  and  specimens.  Rocks,  and  even  their  constituent  miner- 
als, certainly  do  appear  to  the  unaided  eye  to  be  stretched  and  contorted 
without  any  break  in  their  continuity.  Whether,  however,  this  effect 
is  accomplished  by  a truly  molecular  movement,  as  in  a viscous  body, 


1 Xeues  Jahrbucb  flir  Miueralogie,  etc.,  Beilageband  4,  p.  388,  1886. 

2Ibid.,  Beilageband  5,  p.  56,  1887. 

3Zeitechr.  Deutscli.  geol.  Gesell.,  vol.  36,  1884,  p.  858. 

4 Quar.  Jour.  Geol.  Soc.  London,  vo).  42,  1886,  Proc.,  p.  95. 

6 Ibid.,  p.  64. 

6 Ibid.,  p.  65. 


williams.]  DEFORMATION  OF  ROCKS  WITHOUT  RUPTURE. 


47 


or  by  a breaking  or  crushing  of  the  component  crystals  with  a move- 
ment in  the  mass  before  it  is  recemented,  is  something  that  can  not 
be  well  decided  by  the  unaided  eye.  Such  authorities  as  Giimbel1  and 
Pfaff2  at  once  took  exception  to  the  conclusions  of  Heim,  and  stated  it 
as  their  conviction  that,  strictly  speaking,  there  was  no  such  thing  as 
the  deformation  of  rocks  without  rupture.  Baltzer3  could  not  decide 
between  the  conflicting  views,  but  thought  there  was  probably  truth 
in  each.  The  microscopical  study  of  such  bent  and  contorted  rocks 
seems  to  show  that  the  explanation  of  Giimbel  is  generally  the  true  one. 
This  was  emphasized  by  J.  Lehmann.4  He  calls  attention  to  the  fact 
that  the  conception  of  plasticity  is  not  a simple  one.  We  speak  both 
of  wax  and  of  wet  clay  as  “ plastic,”  and  yet  the  movement  of  the 
homogeneous  body  is  different  from  that  in  the  heterogeneous  substance. 
In  each  the  process  of  the  deformation  escapes  the  eye  and  the  results 
appear  the  same;  but  in  reality  the  first  is  molecular,  the  second 
caused  by  the  slipping  of  the  component  particles  (kaolin  scales)  over 
each  other.  In  rocks  the  “plasticity”  is  of  the  second  kind.  Lehmann5 
says: 

When  rock-deformation  has  been  accomplished  by  a breaking  and  sliding  of  the 
individual  constituents  upon  each  other,  I think  that  I am  still  justified  in  calling  it 
a deformation  without  rupture,  provided  the  continuity  of  the  rock-mass  itself  has 
been  preserved  and  no  fissures  have  been  formed.  * * * I recognize  only  that  as 

rock-deformation  with  rupture  when  fissures,  even  though  microscopic,  traverse  the 
rock  independent  of  the  individual  constituents.6 

Again  he  says  :7 

A plastic  molding  of  the  separate  constituents,  as  is  assumed  by  Heim,  I have 
nowhere  been  able  to  discover.  On  the  other  hand,  the  maximum  of  resistance 
which  a crystalline  grain  can  offer  to  bending  or  crushing  is  very  soon  reached,  and 
then  ensues  a pulverizing  or  chemical  solution.8 

Lehmann  also  particularly  emphasizes  the  importance  of  the  very 
much  increased  chemical  action  which  such  a crushing  of  the  rock 
components  permits.  This  had  heretofore  been  almost  overlooked  by 
all  the  students  of  dynamic  or  mechanical  metamorphism  except  Lossen. 
The  ease  with  which  a ready  circulation  and  changed  physical  condi- 
tion allow  the  destruction  of  certain  chemical  compounds,  and  the  iin- 

1 Das  Verhalten  tier  Schichtgesteine  in  gebogenen  Lagen.  Sitzungsberichto  dor  bon.  bayriscben 
Akademie.  Math.-phys.  Claase,  vol.  4,  p.  596,  1880  {reviewed  by  Rosenbuseh  in  the  Neues  Jahrbuck 
fur  Mineral..  1882,  vol.  1,  Referate,  p.  221). 

2 Der  Mechanismus  der  Gebirgsbilduug.  neidelberg,  1880,  p.  140. 

3 Die  mechaaiache  Contact  von  Gneiss  uud  Kalk  irn  Berner  Oborland,  Bern,  1880,  p.  240. 

4 “ Untcrsuchungen  iiber  die  Entstehung  der  altkryatalliniscLien  Scbiefergeateine,  etc..”  Chap.  xvr. 

5 Ibid.,  p.  245. 

°Ich  glaubo  aogar  mit  Recht  eino  Gostoinsformung,  bei  welcbcr  nur  die  einzelnen  Gemongtheile 
zcrapalten  und  aich  an  einander  verschiebon,  ala  eino  bruchloso  bezoickneu  zu  kduen,  weuu  daa 
Geatein  seiner.  Zusammenhalt  bewahrt  hat  uiul  koine  das  Gestoin  durchsttzenden  Risso  vorhanden 
sind.  * * * Eino  Gesteinsformung  mit  Brucli  erkeune  ich  erst  d&tm  an,  wenn  Risso,  und  indgen  os 
auch  mikroskopischesein,  unbekummert  uni  die  Einzelgeincngthoilodaa  Gcatoinagowebodurchsetzen. 

7 Ibid.,  p.  240. 

®Einc  plastiache  Formungder  Einzelgomongthoilo,  wie  aio  Heim  annohmon  zu  miiasen  glaubt,  habo 
icli  niemals  gefunden  ; vielmehr  erreicbt  die  Biegung  oder  Zusamnu  ndi  uckung  cinoa  Krystallkorns 
Behr  bald  daa  Maximum  uud  erfolgt  daun  eino  Zertrurnmorung  bozichungaweiso  auch  eiue  ckemiscko 

Aufliisung. 


48 


GREENSTONE  SCHIST  AREAS  OF  MICHIGAN. 


[BULL.  62. 


mediate  formation  of  others  out  of  their  elements,  is  calculated  to  pre- 
serve the  continuity  of  tlie  rock-mass  in  spite  of  extensive  stretching 
or  compression. 

Such  chemical  changes  will  form  the  subject  of  the  following  section. 
Here  we  are  concerned  only  with  the  mechanical  deformation  of  the 
elementary  minerals. 

The  effects  of  pressure  will  naturally  be  first  noticeable  upon  an 
elastic  mineral  like  mica.  A bending  of  the  lamellae  is  well  known  to 
result  frequently  from  even  the  slight  movement  of  an  eruptive  magma 
before  its  complete  solidification.  Wherever,  therefore,  so  sensitive  a 
mineral  presents  no  pressure  effects  when  more  brittle  substances  show 
them,  it  is  fair  to  assume  That  the  mica  has  been  secondarily  developed 
during  the  action  of  the  pressure. 

Harder  minerals,  like  augite  or  feldspar,  under  the  first  action  of 
strain,  before  their  cohesion  is  overcome,  appear  to  have  twinning 
lamellae  developed  in  them  parallel  to  certain  planes — and  most  abun- 
dantly where  the  strain  is  the  most  intense.  To  this  succeeds  a crack- 
ing of  the  crystal,  with  often  a considerable  separation  of  the  parts  and 
a filling  of  the  interstices  by  newly  depositech substance.1  A still  more 
intense  pressure  accompanied  by  a shearing  stress  seems  to  produce  a 
regular  granulation  of  the  larger  crystals,  so  that  around  their  edge 
they  pass  into  a mosaic-like  aggregate  of  fine  interlocking  grains. 
This  process  in  the  case  of  augite,  as  in  the  Saxon  “ Fiaser-Gabbros,” 
is  attended  by  uralitization,  or  the  production  of  secondary  ampliibole. 
The  resulting  structure,  in  which  larger  grains  are  separated  by  a 
finer  mosaic,  has  been  called  by  Tornebohm,  who  observed  it  in  cer- 
tain Swedish  granites,  “mortar-structure”  (“Moitel  Structur”).2  This 
granulation,  with  increasing  strain,  may  exteud  farther  and  farther 
inward  until  finally  the  entire  crystal  is  replaced  by  a fine  mosaic  of 
interlocking  grains.  When  produced  under  the  influence  of  sufficient 
pressure,  it  may,  of  course,  give  rise  to  a pronounced  banded  or  schis- 
tose structure. 

The  action  of  strain  upon  the  hardest  and  most  brittle  of  the  rock- 
forming minerals — quartz — seems  to  result  in  cracking  and  breaking, 
rather  than  in  bending  it.  Crystals  which  appear  in  hand-specimens 
to  be  stretched  out  into  lenses,  are  shown  by  the  microscope  to  be  com- 
posed of  smaller  grains,  more  or  less  difierent  in  their  optical  orienta- 
tion. Of  this  mineral  Lehmann  says:3 

The  phenomena  which  the  quartz  of  stretched  rocks  exhibit  manifest  themselves 
under  the  polarizations  microscope  in  the  unequal  extinction  of  dilfereut  fields,  and 

1 See  Lehmann's  Atlas,  PI.  6,  Figs.  3,  6,  and  PI.  21,  Figs.  3,  6. 

2Nagra  ord  om  granit  och  gneis.  Geol.  Foreningens  Stockholm  Forhandl.,vol.  5,  pp.  233-248,  1880- 
81  (review  in  the  Roues  Jahrbuch  fur  Mineral.,  1881,  vol.  2,  Referate,  p.  50).  Tornebohm,  in  this 
paper,  considers  this  as  an  original  structure.  Kjerulf  designates  all  such  dynamic  changes  as  are 
manifested  in  a movement  among  the  fragments  of  broken  crystals  as  “ Kataklas-structur."  He  dis- 
tinguishes three  grades  of  intensity.  See  Grundfjeldsprofilet  ved  Mj^scns  sydendo.  Nyfc  Mag.  for 
Naturvidenskaberne,  vol.  29,  p.  215,  1885  (review  Neues  Jahrbuch  fur  Mineral.,  1886,  vol.  2,  Refer- 
ate, p.  244).  See  also  Rosenbusch : Mikros.  Physiog.,  vol.  2,  2d  cd.,  p.  42, 1887. 

*TJntersuchungen  fiber  dio  Entsteliung  der  altkrystalliuischen  Schiefergesteine,  etc.,  p.  250, 


WILLIAMS.] 


DEFORMATION  OF  QUARTZ. 


49 


then  in  a somewhat  more  exact  separation  of  these  fields.  We  imagine  that  we  can 
detect  sharp  boundary  lines  without  being  able  to  certainly  prove  their  existence 
(and  in  reality  they  are  due  merely  to  tension).  Finally,  however,  the  individual 
grain  does  really  break  up  into  separate  interlocking  parts,  which  at  first  are  but 
slightly  chauged  in  their  orientation.  Nevertheless,  toward  the  edge  and  in  the 
more  compressed  portions  these  parts  are  quite  irregularly  orientated  and  participate 
in  the  composition  of  the  ground  mass.  True  bending  of  quartz  is  unknown  to  me. 
It  is  shattered  very  easily,  and,  as  it  seems,  is  as  readily  subject  to  chemical  solution.1 

Prof.  Oh.  E.  Weiss,  of  Berlin,  describes  remarkably  deformed 
quartzes  in  the  schistose  porphyries  occurring  in  the  almost  horizontal 
mica  schist  near  Thai  in  Thuringia.2  This  rock  forms  dikes  which  cut 
across  the  bedding  of  the  schist  and  send  apophyses  in  a horizontal 
direction  between  its  layers.  The  schistose  structure  of  the  porphyry 
was  formerly  considered  to  be  a flow  structure,  but  Weiss  has  shown 
that  this  can  not  possibly  be,  as  it  runs  in  every  case  parallel  to  the 
bedding  of  the  mica-schist  without  reference  to  whether  this  is  parallel  or 
perpendicular  to  the  walls  of  the  dike . The  porphyritic  quartz  crystals  in 
these  rocks  are  drawn  out  into  long,  pear-shaped  or  tadpole-like  (“kaul- 
quappenahulich”)  forms,  which  follow  the  direction  of  the  schistose 
structure.  This  is  accomplished  sometimes  with,  sometimes  without,  a 
rupture  of  the  quartz  substance,  and  produces  what  Lossen  calls  tailed- 
quartzes.  (“  Schwanzchen-quarz.”)3 

It  is  remarkable  that  the  porphyritic  feldspar  crystals  of  these 
rocks  have  suffered  far  less  deformation  than  the  much  harder  quartzes, 
an  observation  which,  as  we  shall  see,  is  abundantly  substantiated  iu 
the  schistose  porphyries  of  the  Lake  Superior  region.  The  phenomena 
exhibited  by  the  Thuringian  rocks,  although  left  without  explanation 
by  Weiss,  are  referred  without  hesitation  by  Rosenbusch  to  the  effects 
of  dynamic  metamorphism.4 

Rosenbusch  also  remarks  that,  as  a rule,  the  peripheral  granulation, 
(“randliche  Kataklase”),  characteristic  of  the  coarse-grained,  granitic 
rocks,  is  wanting  in  the  porphyries.  This  he  attributes  to  the  structure, 
for  in  the  granular  rocks  under  great  pressure  the  grains  rub  against 
each  other,  while  in  porphyritic  rocks  the  larger  crystals  are  imbedded 
in  a homogeneous  matrix,  so  that  they  are  either  only  optically  dis- 
turbed or  completely  pulverized.5 

1 Die  Erscbeinungen,  wolche  der  Quarz  gestreckter  Gesteine  zeigt,  bekundeu  sich  unter  dem  Po- 
larisationsmikroskop  in  einem  ungleiohen  Dunkelwerden  verscbiedenor  Felder,  dann  in  oiner  schar- 
feren  Abgrenzuug  derselben ; man  glaubt  Begrenzungslinien  zu  sehen,  obne  dass  solche  thatsacli- 
lich  nachzuweisen  warcn  — aie  beruhen  wobl  nur  auf  Spannungen— endlieli  zerfallt  das  einlioitliclio 
Korn  aber  wirklich  in  einzelne,  zackig  begrenzte  Tlieile,  dio  zunachst  nur  wonig  aus  ihrer  Lago 
gedrelit  erscheinen  ; gegen  den  Rand  des  Korns  und  in  starker  gepressten  Tlieilen  jedoch  wirr  durch- 
einanderliegen  und  an  der  Zusammensotzuugder  feinkdrnigeu  Grundraassosich  bethciligen.  Eigent- 
liche  Biegungen  von  Quarzon  sind  mir  nicht  bekannt ; er  zerstiickt  und  zerfallt  sehr  leiclit  und 
erliegt  wie  es  scheint  ebonso  leicht  einer  chomischon  Aufldsung. 

2 Jahrbuch  preuas.  geol.  Landesanstalt  fur  1883,  pp.  213-237,  Berlin,  1884;  and  Zoitsch.  Deutsch. 
geol.  Gesell.,  vol.  36,  1884,  p.  858.  Cf.  J.  G.  Bornemann:  Jahrbuch  prouss.  geol.  Landesanstalt  far 
1883,  pp.  383-409,  Berlin,  1884. 

* Zeitscli.  Deutscb.  geol.  Gesell.,  vol.  34,  1882,  p.  C78. 

4 Die  massigon  Gesteine,  2d  ed.,  1886,  p.  214. 

6 Ibid.,  p.  413. 

Bull.  62 4 


50 


GREENSTONE  SCHIST  AREAS  OF  MICHIGAN. 


(BULL.  62. 


Dr.  C.Chelius  describes  compressed  and  schistose  granite  porphyries 
from  the  northern  portion  of  the  Oden  wald  (Hesse-Darmstadt).  In  these 
the  ground-mass  is  quite  fine-grained,  but  where  small  areas  of  it  have 
been  protected,  as  it  were,  by  large  porphyritic  crystals  it  has  nearly 
ticice  as  coarse  a grain,1 

It  would  appear  to  be  quite  generally  the  case  that  porphyritic 
massive  rocks,  when  subjected  to  great  pressure,  develop  the  so-called 
u Augen  structure.”  The  larger  crystals  are  only  partially  pulverized, 
and  have  on  either  side  of  them,  in  the  direction  of  the  schistose  struct- 
ure, a mosaic  of  their  own  debris,  arranged  like  the  “ crag-and-tail  ” of 
a glaciated  ledge.  This  has  been  observed  and  admirably  described  by 
Lehmann2  in  the  Saxon  granulites,  by  Teall3  in  the  gabbros  of  the 
Lizard  district,  Cornwall,  and  by  JBonney.4 

Miner alogical  metamorphism. — This  is  undoubtedly  the  most  impor- 
tant phase  of  metamorphism  in  eruptive  as  well  as  in  sedimentary  rock 
masses.  It  always  accompanies  such  mechanical  deformation — whether 
macroscopical  or  microscopical — as  has  been  already  described ; but, 
while  such  dynamic  processes  may  greatly  facilitate  chemical  action  or 
molecular  rearrangement,  they  are  by  no  means  always  necessary  to 
bring  them  about.  The  adjustment  between  the  chemical  combina- 
tions and  external  conditions  is  so  delicate  in  the  inorganic  world  as 
to  make  the  difference,  in  this  respect,  between  minerals  and  living  or- 
ganisms seem  rather  one  of  degree  than  of  kind.  This  point  has  been 
elaborated  by  Professor  Judd  in  his  recent  annual  address  before  the 
Geological  Society  of  London  (February  18,  1887).5  Wadsworth6  has 
also  insisted  that  the,  changes  in  the  mineral  world  are  due  to  the  pas- 
sages from  states  of  less  stable  to  those  of  more  stable  equilibrium ; 
but,  as  Judd  justly  remarks,  the  cycle  of  changes  may  be  infinite  because 
the  stability  of  a compound  depends  upon  its  surrounding  conditions. 
With  a change  of  these,  a state  which  was  once  stable  becomes  unstable. 
No  student  of  mineralogy  can  fail  to  appreciate  the  extreme  delicacy 
of  the  equipoise.  Any  one  who  has  produced  artificial  twinuing-lamellae 
in  feldspar  or  calcite,  or  watched  sulphur  or  boracite  or  tridymite  or 
leucite  pass  from  one  modification  into  another,  must  acknowledge  the 
importance  of  paramorphism  in  the  formation  of  rocks.  But  changes 
of  minerals  accompanied  by  changes  in  the  chemical  nature  of  the  com- 
pound are  still  more  common.  These  may  consist  (1)  in  the  breaking  up 
of  one  molecule  into  two  or  more,  with  but  little  replacement  of  sub- 
stance, as  in  the  formation  of  saussurite  from  labradorite,  or  of  spodu- 
mene  (aibite  + eucryptite)  from  spodumene;  or  (2)  in  a reaction  which 
takes  place  between  two  contiguous  minerals,  each  supplying  a part  of 

1 Notizblatt  des  Vereins  fur  Erdkundo  z u Darmstadt,  4.  Folge,  Heft  5,  1885,  p.  20. 

2TTntersuchungen  iiber  die  Eutstehung  der  altkrystallinischen  Schiefergesteine,  etc.  Bonn,  1884. 

3Geol.  Mag.,  London,  Nov.,  1886. 

4 Presidential  address  to  the  Geological  Society,  Feb.,  1886.,  Quart.  Jour.  Geol.  Soc.  London,  vol.  42, 

Proc.,  p.  96. 

6 See  also  the  writer,  Top.  Sci.  Monthly,  Sept.,  1889. 

6 Nature,  March  3,  18S7,  p.  417. 


WILLIAMS.] 


MINERALOGICAL  METAMORPHISM. 


51 


the  substance  necessary  to  form  a new  compound  of  intermediate  com- 
position, more  stable  for  the  then  existing  conditions  than  either.  Such 
a case  is  the  formation  of  a hornblende  zone  between  crystals  of  olivine 
or  hypersthene  and  plagioclase,  or  of  the  so-called  u kelyphite”  zone 
between  pyrope  and  serpentine;  (3)  in  more  complicated  and  less 
easily  understood  chemical  reactions,  like  the  formation  of  garnet  or 
mica  from  materials  which  have  been  brought  together  from  a distance 
and  under  circumstances  of  which  it  is  at  present  impossible  to  state 
anything  with  certainty. 

All  such  changes  involving  an  actual  change  in  the  chemical  com- 
- position  are  best  designated  in  contrast  to  those  produced  by  para- 
morphism,  as  metasomatic.1 

Of  course  all  of  these  metamorphic  changes  of  a mineralogical  char- 
acter— whether  paramorphic  or  metasomatic — may  go  on  in  all  conceiva- 
ble proportions  in  a rock  mass  at  the  same  time.  They  are  often 
accompanied  by  changes  in  the  original  structure  of  the  rock,  but  not 
of  necessity,  although  such  changes  of  structure  can  not  be  accom- 
plished without  chemical  alteration. 

Chemical  changes  in  minerals  and  rocks  have  occupied  the  attention 
of  mineralogists  and  chemists  from  the  beginning  of  the  century,  and 
yet  it  is  almost  exclusively  in  sedimentary  rocks  that  such  studies  have 
been  carried  on.  Only  within  recent  years  have  the  mineralogical  met- 
amorphoses which  take  place  in  eruptive  rocks  commenced  to  receive 
their  proper  share  of  consideration.  Lossen,  Tornebohm,  and  J.  Leh- 
mann.were  the  first  in  Europe  to  recognize  the  importance  of  such  in- 
vestigations; while  it  will  ever  remain  one  of  the  most  signal  services 
which  Dr.  Wadsworth  has  rendered  to  petrography  that  he  was  the 
first  in  America  to  fully  grasp  their  significance  and  to  emphasize  it. 

It  would  be  quite  beyond  the  purpose  of  the  present  paper,  even  if 
it  were  possible,  to  give  a complete  summary  of  all  that  has  been  done 
on  the  subject  of  chemical  changes  in  eruptive  rocks.  In  this  place  the 
attempt  will  be  made  only  to  trace  out  historically  some  of  the  more 
important  alterations  which  have  a direct  bearing  upon  the  rocks  form- 
ing the  subject  of  this  investigation.  Important  and  wide-spread  phases 
of  the  metamorphism  of  eruptive  rocks — such,  for  instance,  as  serpen- 
tinization — which  are  not  exemplified  within  the  area  studied  will  not 
be  here  considered.  On  the  other  hand,  minor  details  or  local  modifi- 
cations of  well  known  and  universally  recognized  processes  will  be  elab- 
orated in  the  course  of  the  special  petrographical  descriptions  (Chap- 
ters II-V)  and  summarized  in  Chapter  VI. 

The  points  which  will  be  historically  considered  in  this  chapter  are 
t lie  following : 

( l.)Uraliiization , or  the  secondary  origin  of  hornblende,  both  fibrous 
and  compact,  from  pyroxene. 

1 This  term  is  preferred  to  mcthylosig  of  Kin"  and  Rownoy  (“An  old  chapter  of  the  geological  record 
with  a new  interpretation;"  London,  1881),  and  Bonney  (Quart.  Jour.  Gool.  Soc.,  London,  vol.  42, 
1886,  Proc.,  p.  59),  and  to  metachemic  of  Dana  (Am.  Jour.  Sci.,  1886,  3d  sories,  vol.  32,  p.  70),  because  it 
is  at  present  so  much  rnoro  widely  used  and  honco  so  much  moro  intelligiblo. 


52 


GREENSTONE  SCHIST  AREAS  OF  MICHIGAN. 


[BULL.  62. 


(2.)  Chloritization. 

(3.)  Fpidotization. 

(4.)  Formation  of  the  viridite  (chlorite)  epidote  aggregate. 

(5.)  Saussuritization. 

(0.)  Formation  of  the  albite  mosaic . 

(7.)  Sericitization. 

(8.)  Alterations  of  titanic-iron. 

Uralitization. — Ever  since  the  classic  record  of  observations  made  by 
Gustav  Rose  in  the  Ural  Mountains  in  1830, 1 the  fact  has  remained  un- 
disputed that  pyroxene  sometimes  changes  to  an  aggregate  of  amplii- 
bole  needles  which  often  preserve  by  their  arrangement  the  original 
augitic  form.  It  was  not  long  before  other  similar  occurrences  were 
discovered,  notably  in  Scandinavia  and  the  Tyrol.  Still,  these  localities 
were  regarded  as  exceptional,  and  it  was  impossible  that  the  full  geo- 
logical importance  of  Rose’s  uralite  should  be  appreciated  without  the 
aid  of  the  microscope.  With  the  help  of  this  instrument  it  was  soon 
discovered  that  the  smaragdite  of  the  saussurite  gabbros  or  euphotides 
was  a secondary  hornblende  which  had  originated  from  the  diallage. 
As  the  number  of  observers  and  observations  increased,  instances  of 
the  undoubted  passage  of  every  sort  of  pyroxene  into  a fibrous  arnphi- 
bole  grew  constantly  more  and  more  abundant.  It  would  be  useless 
to  attempt  "to  trace  out  these  discoveries  in  detail.  It  is  enough  merely 
to  mention  the  names  of  Rose,  Vom  Rath,  Fischer,  Hagge,  Zirkel,  Von 
Lasaulx,  Rosenbusch,  Tornebohm,  Svedmark,  Sjogren,  Becke,  Kioos, 
Micliel-L6vy,  Allport,  Phillips,  Teall  and  Hatch,  in  Europe,  and  of 
Hawes  in  this  country,  to  recall  the  accuracy  and  value  of  the  facts  re- 
corded, while  among  the  first  to  see  further  than  mere  facts  and  to  grasp 
the  full  geological  significance  of  this  wide-spread  change  may  be  placed 
Lossen,  Lehmann,  Reusch,  Wadsworth  and  Irving. 

The  alteration  of  pyroxene  to  hornblende  is  almost  universally  alluded 
to  as  paramorphism,  and  such,  indeed,  it  may  be  in  some  instances. 
Still,  many  investigations  go  to  prove  that  it  is  very  often,  perhaps  al- 
ways, accomplished  by  chemical  change.  The  original  uralite  of  Rose 
was  too  soft  and  hydrous  to  be  compared  with  hornblende.  The  studies 
of  Forschhammer,  Rose,2  and  Svedmark3  showed  that  when  augite 
changed  to  fibrous  hornblende,  magnetite  and  often  calcite  was  sepa- 
rated out  between  the  needles.  A recent  opinion  by  Rosenbusch  on 
this  point  is  as  follows : 

This  uralitization  can  hardly  he  regarded  as  a simple  act  of  molecular  rearrange- 
ment; we  should  rather  expect  that  apart  of  the  lime  contained  in  the  augite  would 
pass  into  other  combinations,  and,  in  fact,  epidote  is  an  almost  constant  companion 
of  uralite.4 

1 Poggendorff  Aniialen,  vol.  22,  1831;  vol.  31,  1834,  p.  G17;  al&o  Iieise  nacb  dein  Oral,  vol.  2,  p.  342. 

2Zeit8clir.  Deutscb.  gool.  Gesell.  Berlin,  vol.  16,  1864,  p.  6. 

3Neues  Jabvbucb  fur  Mineral.,  1877,  p.  99;  Mikros.  Pliysiog.,  vol.  2,  2d  ed.,  p.  185;  vol.  1,  p.  472. 

4Diese  Uralitisirung  kann  nicht  wobl  oin  einfacber  Act  raolecularer  Uralagerung  sein,  es  ist  viel 
mebr  zu  erwarten,  dass  ein  Tk6il  ties  Kalkgebalts  des  Augits  in  andero  Verbindungen  iibergeho  und 
tbatsachlicb  ist  Epidot  ein  nabezu  constanter  Begleiter  des  Uralits. 


WILLIAMS.] 


UEALITIZATION 


58 


Dr.  B.  Harrington,  of  Montreal,  has  carefully  analyzed  three  stages 
of  alteration  between  pyroxene  aud  a secondary  fibrous  hornblende 
resulting  from  it,  and  has  found  that  during  the  change  there  has  been 
a great  loss  of  lime  and  a gain  of  magnesia,  silica,  and  the  alkalies.1 
The  specimen  investigated  was  one  of  the  excellent  examples  of  uralite 
from  the  apatite  mines  near  Ottawa,  Canada,  similar  to  those  named 
by  Thomson  “ Rapliilite.”  2 

Mr.  J.  J.  H.  Teall  has  also  recently  discussed  this  point  in  connec- 
tion with  his  studies  of  the  alteration  of  the  Scourie  dike,3  and  is  of  the 
opinion  that  the  oxidation  of  iron  from  the  ferrous  to  the  ferric  state  is 
incident  to  the  change  of  augite  to  hornblende. 

While  the  alteration  of  almost  any  pyroxene  into  fibrous  hornblende 
has  now  become  a universally  recognized  fact,  the  possibility  of  the 
chaugeof  this  mineral  directly  into  compact  hornblende  is  by  no  means 
so  generally  admitted.  So  admirable  an  observer  as  J.  H.  Kloos  has 
recently  based  his  distinction  between  primary  and  secondary  aiuphi- 
bole  in  the  Black  Forest  gabbros  entirely  upon  their  compact  or  thin 
fibrous  character.4  Still,  the  work  of  many  investigators  shows  that 
this  is  by  no  means  a reliable  criterion  in  all  cases. 

Svedmark  found  in  187I)  that  the  pyroxene  of  the  Yaksala  porphyry 
passed  into  an  aggregate  of  stout,  compact  amphibole  needles.5  In 
1877  Streng  described  compact  brown  hornblende  in  the  Minnesota 
gabbros,  which  he  considered  to  have  originated  from  the  diallage;6 
and  in  1878  Dr.  George  W.  Hawes  described  and  figured  similar  occur- 
rences in  certain  New  Hampshire  rocks.7  In  1880  appeared  accounts 
by  Irving,  and  in  1882  by  both  Irving  aud  Yan  Hise,  of  compact  brown 
hornblende  originating  from  diallage.8  In  1880  C.  von  John  described 
the  alteration  of  diallage  to  compact  brown  hordblende  in  the  olivine 
gabbro  of  Bosnia.9  In  1883  Hj.  Sjogren  regarded  the  irregular  spots 
of  compact  brown  hornblende  which  occur  in  and  around  the  pyroxene 
of  the  wernerite  or  dipyre-diorite  of  Bamle  in  Norway  as  produced  by 
a molecular  rearrangement  of  the  pyroxene  substance.10  In  1884  similar 
observations  were  made  by  myself  in  certain  pyroxenites  of  the  “ Oort- 
landt  Series,”  occurring  at  Montrose  Point  on  the  Hudson  River;  also 
in  the  so  called  u black  granite”  (gabbro)  from  Addison,  Me.,  and  in 
rocks  from  the  apatite  regions  of  Canada.11  In  the  same  year  (1884) 

‘Geol.  Survey,  Canada.  Keport  of  progress  for  1878-79.  Appendix  G,  p.  23. 

2 Outlines  of  Mineralogy,  Geology,  etc.,  London,  1836,  vol.,1,  p.  153. 

8 Quart.  Jour.  Geol.  Soe.  London,  vol.  41,  1885,  p.  137. 

4Ncuc8  Jahrhncli  fur  Mineral.,  Beilage-Band  3,  1884,  pp.  32,  33. 

6 Geol.  Fbrcningens  Stockholm  Fdrhandl.,  1876,  pp.  151-164 ; Neues  Jalirbuch  fiir  Mineral.,  1877,  p.  99. 

6Ncucs  Jahrbuch  fiir  Mineral.,  1877,  pp.  133,  240;  Am.  Jour.  Sci.,  Dec.,  1884,  p.  4C4. 

7 The  Geology  of  New  Hampshire,  vol.  3,  1878,  j>art  iv,  Mineralogy  and  Lithology,  pp.  57,  206,  pi.  vii, 

fig  1. 

8Gool.  Wisconsin,  vol.  3,  (1880)  p.  170;  vol,  4,  (1882)  p.  662.  See  also  Geol.  Wisconsin,  vol.  1, 1883,  p. 
321,  and  Am.  Jour.  Sci.,  3d  series,  vol.  26.  p.  29,  1883. 

•Grundlinien  der  Geologic  von  Bosnieu- Herzegovina*  Wien,  1880.  (Cf.  Neues  Jalirbuch  fiir  Mineral., 
1881,  vol.  2.  Ileferate,  p.  353.) 

10 Geol.  Fdreniugens  Stockholm  FfSrhnndl.,  vol.  6,  p.  447,  1883.  (Cf.  Neuos  Jahrbuch  fiir  Mineral. 
1884,  vol.  1.  Keferate,  p.  81.) 

11  Am.  Jour.  Sci.,  3d  series,  vol.  28,  Oct.,  1884,  p.  261. 


54 


GREENSTONE  SCHIST  AREAS  OF  MICHIGAN. 


[BULL.  62. 


A.  Sckenck  quotes  in  his  Inaugural  Dissertation  a statement  made  by 
von  Lasaulx  in  1878,  that  pyroxene  passes  first  into  fibrous  and  subse- 
quently into  compact  brown  hornblende.1  Sckenck  himself  observed  in 
the  Rimberg  diabase  from  the  upper  Ruhr  Valley  that  the  reverse  of 
this  was  true,  i.  e.,  that  the  pyroxene  passed  first  into  compact  brown, 
and  this  subsequently  into  fibrous  green  hornblende.2 

The  secondary  hornblende,  so  well  described  and  figured  by  Teall  in 
the  Scourie  dike,  is  decidedly  compact  in  its  nature,3  nor  is  that  derived 
from  the  paramorphism  of  the  diallage  in  the  Saxon  u flaser-gabbros,” 
according  to  the  observations  of  J.  Lehmann,  less  compact.4  Such 
eminent  authorities  as  Lossen5  and  Rosenbusch6  also  allow  that  there  is 
no  doubt  that  compact  basaltic  hornblende  occasionally  results  through 
the  direct  paramorphism  of  diallage,  or  even  orthorhomi  ic  pyroxene. 
The  chemical  composition  of  the  original  mineral  undoubtedly  largely 
conditions  the  nature  of  the  resultant  product.  This  is  shown  by  the 
observations  of  vou  John  in  the  Flysch-gabbros  of  Bosnia,  where  brown 
hornblende  resulted  from  dark  and  green  hornblende  from  pale  diallage.7 

These  facts  are  dwelt  upon  here  somewhat  in  detail  because,  as  will 
been  seen  in  the  sequel,  they  have  possibly  an  important  bearing  on  a 
large  part  of  the  Menominee  River  greenstones. 

It  is  not  intended,  of  course,  to  imply  by  the  above  statements  that 
true  parallel  growths  of  primary  augite  and  primary  brown  hornblende 
may  not  occur,  as  held  by  both  Lossen  and  Rosenbusch  (loo.  cit.). 
Such  parallel  growths  would  have  the  closest  possible  resemblance  to 
alteration  forms,  and  I can  not  escape  the  conviction  that  the  tendency 
of  future  studies  will  be  to  attribute  a secondary  origin  to  more  and 
more  of  such  intergrown  brown  hornblende. 

The  derivation  of  fibrous  or  actinolitic  hornblende,  quite  identical  in 
all  respects  with  uralite,  from  compact  hornblende  (whether  brown  or 
green)  seems  hitherto  to  have  been  much  neglected.  luostrauzeff  in 
1879  described  Russian  diorites  in  which  the  original  hornblende  had 
passed  into  secondary  aetinolite,  as  well  as  into  biotite,  chlorite  and 
talc.8  Becke  also,  in  1882,  mentions  uralite  formed  from  both  pyroxene 
and  compact,  primary  hornblende,  in  the  kersantite  of  the  “Nieder- 
oesterreicliisckes  Waldviertel.” 9 

Descriptions  have  also  been  given  by  myself  of  compact  brown  horn- 
blende changing  into  the  green  fibrous  variety  in  the  Baltimore 
gabbros.10 

1 Verli.  (1.  naturh.  Vereins  d.  pr.  Rlieinl.  und  Westf.,  1878,  p.  171,  pi.  iv,  fig.  4. 

2 Die-Diabase  des  oberen  Rulirthals,  etc.,  Inaugural-Dissertation.  Bonn,  1884,  p.  41. 

3 Quart.  Jour.  Geol.  Soc.  London,  vol.  41,  p.  137,  1885,  pi.  II,  fig.  2. 

4T7eber  die  Entsiehung  der  altkrystallinischcn  Schiefergesteine,  etc.  Bonn,  1884. 

6 Jahrbucli  preuss.  geol.  Landesanstalt  fiir  1884,  p.  537,  Berlin,  1885. 

6Mikros.  Pliysiog.,  2d  ed.,  vol.  2,  1887,  pp.  141,  209. 

7TJeber  kryst.  Gest.  Bosniens  und  der  Herzegovina  in  Grundlinien  der  Geol.  von  Bosnien -Herzego- 
vina, Wien,  1880  (ref.  Nenes  Jahrbucli  fiir  Mineral.,  1881,  vol.  2.  Referate,  j>.  353). 

8Studien  fiber  inetainorphosirte  Gesteine  im  Gouvernement  Oloncz.  Leipzig,  1879  ( cf . Neues  Jabr- 
bucli  fiir  Mineral.,  1880,  vol.  2.  Referate,  p.  342). 

9Tschermak’8  mineral,  u.  petrog.  Mittheil.,  vol.  5,  1883,  pp.  157-159. 

10  Bull.  U.  S.  Geol.  Survey,  No.  28,  p.  45. 


WILLIAMS.] 


CHLOR1TIZATION. 


55 


The  common  alteration  of  rock-forming  hornblende  appears  to  be  to 
chlorite  or  to  epidote,  or  into  an  aggregate  of  both  these  minerals. 
This  is  almost  the  only  change  mentioned  by  Rosenbusch  in  his  most  re- 
cent works,  although  in  one  place  he  says : il*  * * bei  Chloritisirung 

fasert  sicli  die  Hornblende  aus  * * * ” etc.1  That  this  change  of 
compact  to  fibrous  hornblende  is,  however,  of  great  importance,  the  rocks 
described  in  the  sequel  will  abundantly  prove. 

Chloritization. — An  admirable  exposition  of  the  present  state  of  our 
knowledge  relative  to  the  so-called  “chloritic  constituent”  of  the  dia- 
bases and  allied  rocks  is  to  be  found  in  the  most  recent  work  of  Rosen- 
busch.2 The  secondary  hydrous  minerals  of  a green  color,  whose  almost 
universal  presence  has  brought  to  this  whole  class  of  rocks  the  gen- 
eral designation  ‘‘greenstone,”  owe  their  existence  to  the  processes 
known  as  weathering,  rather  than  to  such  as  may  be  strictly  called  met- 
amorphic.  There  can  be  but  little  doubt  that  they  have  been  formed 
mainly  out  of  the  components  of  the  pyroxene,  although  these  wander 
so  during  the  process  of  the  alteration  that  the  new  products  by  no 
means  occupy  the  exact  position  of  the  original  mineral.  It  seems  pos- 
sible to  distinguish  two  classes  of  such  secondary  substances : First, 
such  as  are  more  or  less  fibrous  in  structure,  without  pleochroism,  and 
have  a decided  action  upon  polarized  light;  and,  second,  such  as  are 
scaly  in  structure,  with  pleochroism  and  so  weakly  polarizing  as  to 
appear  isotropic.  The  first  class  embraces  substances  allied  to  serpen- 
tine; the  second,  those  which  more  or  less  closely  resemble  chlorite. 
In  certain  cases  they  have  been  chemically  identified  with  such  indefi- 
nite species  as  delessite,grengesite  (Hisinger),  seladonite,  chloroplneite 
(Macculloch),  epichlorite  (Rammelsberg),  diabantachronnyn  (Liebe),3 
and  diabantite  (Hawes).4  All  of  these  substances  resemble  each  other 
more  or  less  closely  in  both  physical  and  chemical  behavior,  and  I am 
inclined  to  agree  with  Rosenbusch5  in  preferring  the  generic  term 
u chlorite ” or  “ chloritic  substance ” for  them,  to  even  the  indefinite  des- 
ignations “ viridite ” of  Vogelsang6  or  u chloropite”  of  von  Giimbel.  In 
fact  Keungott  has  shown  that  the  formula  of  diabantachronnyn  may 
be  brought  quite  into  accord  with  that  of  typical  chlorite.7 

Liebe  found  the  greenish  coloring-matter  of  the  dark  titanic  iron 
diabases  of  Voigtland  and  Frankenwald  to  be  picrolite  (serpentine),  and 
it  is  not  unusual  to  observe  the  curious  vermicular  aggregates  of  cir- 
cular chlorite  scales  to  which  Volger  has  given  the  name  helminth.8 

It  is  well  known  that  the  results  produced  by  the  weathering  of  horn- 

1 Mikros.  Physiog.,  2d  ed.,  vol.  2,  1887,  pp.  468,469. 

2 Ibid.,  pp.  180-184. 

*Neues  Jahrbuch  fur  Mineral.,  1870,  p.  2. 

4 Am.  Jour.  Sci.,  3d  series,  vol.  9, 1875,  pp.  454-457 ; Geol.  Now  Hampshire,  vol.  3,  part  3 ; 1878,  p.  120. 

6 Mikros.  Physiog.,  2d  ed.,  vol.  2, 1887,  p.  183. 

c Archives  N6erlandaisos,  vol.  7,  1872;  Zcitscb.  Deutsch.  geol.  Gesell.,  vol.  21,  1872,  p.529. 

7Neues  Jabrbuch  fiir  Mineral.,  1871.  p.  51. 

8Studien  zur  Entwickeluugsgeschichto  der  Mineralion,  1854,  p.  142. 


56 


GREENSTONE  SCHIST  AREAS  OF  MICHIGAN. 


[BULL.  62. 


blende  or  mica  are,  in  most  instances,  quite  similar  to  those  just  de- 
scribed in  the  case  of  pyroxene.  Such  a change  of  hornblende  may  have 
an  equal  importance  in  those  greenstones,  like  a large  proportion  of 
those  to  be  considered  in  this  paper,  whose  bisilicate  constituent  was 
originally  augite,  but  which  was  subsequently  changed  by  a truly  meta- 
morphic  process  (uralitization)  to  hornblende  before  the  final  weather- 
ing commenced. 

The  last  result  of  the  action  of  the  atmospheric  influences  upon  the 
chlorite  is,  as  Rosenbusch  long  ago  showed,  to  convert  it  into  an  aggre- 
gate of  limonite,  carbonate,  and  quartz. 

Epidotization. — The  most  careful  and  detailed  observations  on  this 
process  are  to  be  found  in  the  Inaugural  Dissertation  of  Adolf  Sehenck 
on  the  Diabases  of  the  upper  Ruhr  Valley  and  their  Contact  Phenom- 
ena.1 This  investigator  finds  that  certain  of  these  diabases  are  converted 
into  u Epidosites,”  or  aggregates  of  epidote  and  either  quartz  or  calcite. 
He  suggests  the  only  three  possible  hypotheses  for  the  formation  of 
this  epidote,  viz:  (1)  That  it  was  formed  by  the  action  of  the  decomposi- 
tion products  of  the  bisilicate  (mainly  CaO  and  Ee203)  upon  the  feld- 
spar substance ; (2)  That  the  reverse  was  true,  i.  e.,  that  the  decomposi- 
tion products  of  the  feldspar  (mainly  A1203  and  CaO)  acted  upon  the 
pyroxene ; (3)  That  there  was  a mutual  reaction  between  the  decom- 
position products  of  both  the  original  constituents.  The  first  of  these 
hypotheses  is  regarded  by  the  author  as  the  only  tenable  one  for  the 
rocks  which  he  studied,  because  in  all  those  diabases  which  contained 
much  epidote  the  feldspar  was  remarkably  fresh  and  the  pyroxene  de- 
composed, while  in  those  whose  feldspar  was  extensively  altered  epidote 
was  almost  wanting.  Observations  of  the  change  of  feldspar  to  epidote 
are  cited  from  the  writings  of  Dathe,  Cohen,  Rosenbusch,  Liebisch,  von 
Lasaulx,  Inostranzeff,  Zirkel,  Michel  Levy,  Kuhn  and  Scheilitz;  and  even 
more  authorities  are  quoted  to  show  that  this  same  mineral  originates 
from  augite,  or  more  commonly  from  hornblende  or  uralite.  If  iron  is 
not  at  hand,  the  place  of  the  epidote  appears  to  be  taken  in  the  feld- 
spar by  zoisite.  An  excellent  example  of  the  origin  of  epidote  as  a re- 
actionary rim  between  the  substance  of  hornblende  and  plagioclase  has 
been  described  and  figured  by  myself  in  the  Baltimore  gabbros  and  their 
derivatives.  Here  the  epidote  forms  a continuous  border  around  the 
hornblende,  it s crystals  projecting  from  it  outward  into  the  feldspar2 

Viridite  (chlorite)- Epidote  Aggregate. — The  simultaneous  action  of  the 
two  last  described  processes  (chloritization  and  epidotization)  in  an 
aluminous  pyroxene  or  hornblende  results  in  the  production  of  an  ag- 
gregate consisting  of  sharply  defined,  pale  yellow  crystals  of  epidote, 
imbedded  in  a green,  scaly  mass  of  chlorite.  The  appearance  of  this 
under  the  microscope  is  shown  on  PI.  XI,  fig.  1.  The  magnesia,  together 

*Die  Diabase  des  obercn  Rulirthals  und  ibro  Contacterscheinuugen  mit  dem  Lenneschiefer.  Bonn, 
1884. 

2 Bull.  U.  S.  Geol.  Survey,  No.  28,  1880,  p.  32.  PI.  m,  Fig.  2. 


WILLIAMS.] 


THE  CHLORITE  EPIDOTE  AGGREGATE. 


57 


with  a proportion  of  the  iron,  alumina  and  silica,  have  here  formed 
the  chlorite;  while  the  lime,  instead  of  becoming  a carbonate,  as  it  often 
does,  has  become  fixed,  in  combination  with  the  rest  of  the  iron? 
alumina  and  silica,  as  epidote. 

Such  aggregates  have  not  escaped  the  notice  of  petrographical  stu- 
dents, though  curious  mistakes  have  sometimes  arisen  as  to  their  true 
nature  and  origin. 

In  1874  Dathe  described  this  association  of  chlorite  and  epidote  with 
great  correctness  and  precision.  He  says : 

When  secondary  products  become  abundant  and  the  leek-green  viridite  increases 
in  amount  and  distribution,  then  there  are  often  associated  with  this  light  yellow 
crystals,  whose  difference  from  the  viridite  is  very  apparent  under  the  microscope.  In 
the  progress  of  my  studies,  I have  recognized  these  crystals  as  pistazite.1 

In  1876  Zirkel  described  the  change  of  horu blende  to  an  aggregateof 
epidote,  viridite  (chlorite)  and  magnetite,  with  which,  in  many  instances, 
more  or  less  cal  cite  was  associated.2 

In  the  same  year,  Wichmann,  in  his  paper  on  the  iron  rocks  of  the 
south  shore  of  Lake  Superior,  which  was  not,  however,  published  until 
1880, 3 described  this  chlorite  epidote  quite  correctly  in  some  instances, 
although  he  says  that  it  is  beyond  doubt  that  the  epidote  has  been  formed 
out  of  the  viridite.  In  other  cases  he  regards  the  mineral  imbedded  in 
the  viridite  as  a secondary  augite,  which,  as  in  the  last  instance,  he 
thinks  was  formed  from  the  chlorite.  He  says  of  this  :4 
The  phenomenon  of  the  transformation  of  viridite  into  augite  has  not  been  observed 
until  recently.  It  is  very  interesting  to  have  the  fact  established  that  this  mineral, 
after  having  been  changed  into  another,  has  finally  returned  to  its  former  state.  * * * 
Such  individuals  are  only  present  in  viridite  and  do  not  seem  to  occur  in  any  other 
part  of  the  rock. 

George  F.  Becker  in  the  course  of  his  microscopical  studies  of  the 
rocks  of  the  Comstock  Lode,  ^Nevada,  which  were  either  identical  with 
those  investigated  by  Zirkel,  or  very  closely  allied  to  them,  found  the 
same  change  of  bisilicates  to  an  aggregate  of  chlorite  and  epidote  which 
the  latter  observer  had  recorded.  Mr.  Becker  is,  however,  very  posi- 
tive that  the  epidote  has  been  developed  after  and  at  the  expense  of  the 
chlorite,  instead  of  simultaneously  with  it.5  This  he  attempts  to  explain 
upon  chemical  grounds.6  The  improbability  of  Becker’s  supposition 
was  brought  out  by  Rosenbusch  in  a review  of  his  work.7 
In  this,  as  well  as  in  his  more  recent  text-book,8  Rosenbusch  clearly 

1 Wenn  die  Neubildnngsproducte  sich  im  Gestein  haufen,  wenn  der  lauchgriine  Viridit  [ChloritJ  an 
Masse  und  Verbreitung  zunimmt,  stellen  sich  oftmals  neben  letztoren  lichtgelbliche  Gebilde  ein, 
deren  Verscliiedenheit  vom  Viridit  bei  mikroskopischer  Betracbtung  sofort  in  dio  Augen  springt.  Ira 
Verlauf  der  Untorsnclrang  wurdeii  diese  Gebilde  als  Pistazit  erkannt.  Mikroskopischo  Unter 
snehungen  iiber  Diabase.  Zeitsch.  Dentsch.  geol.  Gesell.,  vol.  26,  1874,  p.  16. 

^Microscopical  Petrography,  Washington,  1876,  p.  66,  PI.  ill,  Figs.  2 and  3. 

3 Geol.  Wisconsin,  vol.  3, 1880,  pp.  600-656. 

« Ibid.,  pp.  623,  624. 

“The  Geology  of  the  Comstock  Lode.  Monograph  U.  S.  Geol.  Survey,  vol.  3,  p.  76. 

6 Ibid.,  pp.  211-214. 

7Noues  Jahrbuch  fiir  Mineral.,  1884,  vol.  2.  Referate,  p.  189. 

®Mikros.  Physiog.,  2d  ed.,  vol.  2,  pp.  108, 183. 


58 


GREENSTONE  SCHIST  AREAS  OF  MICHIGAN. 


[BULL.  62. 


shows  that  the  true  deviation  of  the  chlorite-epidote  aggregate  is  to 
be  found  in  a division  of  the  bisilicates  out  of  wThich  it  is  formed, 
the  magnesia  passing  into  the  chlorite  and  the  calcium  and  ferric  iron 
into  the  epidote.  The  triclinic  feldspar  may  often  materially  assist  in 
this  formation  by  furnishing  the  necessary  lime. 

Nor  is  this  mistake  of  Mr.  Becker's  a new  one.  Francke  in  1875  de- 
scribed the  same  mineral  association  and  gave  the  same  explanation  for 
it;1  while  in  1880  Schauf,2  in  1882  Kiemann,3  and  in  1884  Schenck  cor- 
roborated the  observation,  although  both  Schauf  and  Schenck4  raised 
unanswerable  chemical  objections  to  the  derivation  of  the  epidote  from 
the  chlorite. 

Saussuritization. — The  hard,  compact,  whitish  or  greenish  substance, 
without  luster  or  cleavage,  which  forms  one  of  the  two  main  components 
of  the  certain  coarse  gabbros  or  euphotides,  was  called  by  H.  B.  Saus- 
sure,  in  1780,  “jade.”5  In  180G  Th.  Saussure  named  this  mineral,  in 
honor  of  his  father,  “saussurite,6  but  its  true  nature  continued  for  over 
half  a century  to  elude  all  mineralogists.  As  long  as  chemical  analysis 
was  the  only  means  with  which  it  could  be  studied,  any  satisfactory 
solution  of  the  riddle  seemed  to  be  impossible.  Such  investigators  as 
vom  Bath,7  Klaproth,8  T.  Sterry  Hunt,9  and  many  others  obtained  the 
most  diverse  results;  the  composition  in  some  cases  approaching  that 
of  zoisite,  in  others  that  of  garnet,  scapolite,  or  feldspar.  In  186G,  Zir- 
kel  remarked,  at  length,  upon  the  extremely  imperfect  state  of  knowl- 
edge regarding  this  geologically  important  mineral.10 

It  remained  for  the  microscope  to  disclose  the  composite  nature  of 
saussurite  as  well  as  to  point  out  the  true  significance  of  its  origin  and 
occurrence. 

Hagge  was  the  first  to  correctly  describe  saussurite  as  an  aggregate  of 
colorless  or  greenish  crystal  needles,  prisms  or  grains,  irregularly  scat- 
tered through  a colorless,  glassy-looking  matrix.11  He,  however,  retained 
the  name  saussurite  for  the  included  grains,  and  did  not  attempt  to  de- 
termine their  mineral  nature.  Hagge.also  clearly  recognized  that  in  all 
cases  observed  by  him  the  saussurite  was  a product  of  the  alteration  of 
feldspar,  and  that  the  passage  from  one  mineral  to  the  other  was  a grad- 
ual one  which  the  microscope  could  easily  follow.12  These  results  were 

1 Studien  iiber  Corillerengesteine.  Inaugural-Dissertation.  Leipzig,  1875. 

2 Verhl.  d.  nat.  Vereins  d.  pr.  Rheinl.  u.  Westf.,  1880,  p.  6. 

3 Ibid.,  1882,  p.  256. 

4 Inaugural-Dissertation.  Bonn,  1884,  p.  45. 

E Voyages  dans  les  Alpes,  vol.  1,  Neuch&tel,  1779,  p.  83. 

6 Annales  de  chirnie  et  de  physique,  3d  series,  vol.  16,  p.  469. 

7Poggen(lovfF  Annalen,  vol.  95, 1855,  p.  555. 

8Beitrage,  vol.  4,  p.  271. 

9 Am.  J our.  Sci.,  2d  series,  vol.  27, 1 859,  pp.  336-349. 

10  Lelirbucli  der  Petrograpbie,  vol.  1,  p.  27 ; vol.  2,  p.  110, 1866. 

I]  Mikroskopiscbe  Untersuchungen  iiber  Gabbro  and  vorwandte  Gesteino.  Kiel,  1871.  On  p.  51  ho 
says:  “ Der  Saussurit  besteht  aus  kleinen  Krystallnadelu,  Prismen  uml  Kbrneru,  die  tarblos  oder 
blassgriin  sind  und  rogellos  in  einer  wie  ein  farbloses  Glas  aussehenden  Grundmasse,  die  aucli  viel- 
facli  klare  Spalten  in  dem  Saussurit  bildot,  vertbielt  liegeu.” 

12  Ibid.,  pp.  35  and  51. 


WILLIAMS.] 


SAUSSUR1TIZATI0N. 


59 


quoted  by  Zirkel  in  liis  text- book,  published  in  1873.1  The  conclusion 
that  saussurite  was  “an  aggregate  and  probably  the  end  product  of  a 
molecular  rearrangement  in  the  feldspar”  was  also  reached  by  Rosen- 
busch  in  the  same  year.2  In  1878  Becke  showed  that  the  saussurite  of 
certain  Grecian  rocks  was  largely  zoisite  ;3  and  in  18S3  appeared  the  im- 
portant paper  by  Oathrein  upon  this  subject.4  This  author  draws  from 
his  work  the  following  six  conclusions  as  to  the  nature  of  saussurite. 

(1)  The  so-called  saussurite,  far  from  being  a homogeneous  mineral, 
is  an  aggregate  of  plagioclase,  rarely  orthoclase,  with  zoisite.  Actino- 
lite,  chlorite,  and  other  minerals  may  also  occur  as  accessories. 

(2)  The  chemical  composition  of  saussurite  resembles  most  that  of 
the  lime  soda  feldspars  ; it,  however,  contains  less  silica,  more  lime,  and 
has  a higher  specific  gravity. 

(3) '  The  proportions  of  the  saussurite  elements  can  be  calculated  from 
the  amounts  of  alkalies,  lime,  and  iron,  if  we  know  the  species  of  the 
original  feldspar. 

(4)  This  proportion  can  also  generally  be  calculated,  even  when  this 
last  factor  is  unknown,  by  a consideration  of  the  relative  difference  of 
silica,  alumina  and  lime  in  zoisite  and  anortiiite. 

(5)  Saussurite  is  a product  of  the  metamorphism  of  feldspar  through 
an  exchange  of  silica  and  alkali  for  lime,  iron  and  water. 

(6)  The  epidotization  of  feldspar  is  genetically  the  same  process  as 
saussuritizatiou  and  differs  only  in  the  larger  proportion  of  iron  required. 

H.  Reusch  considered  the  saussurite  which  composed  a large  part  of 
the  Bergen  gabbros  as  partly  epidote,  partly  zoisite.5  Traube  found 
the  structure  and  composition  of  the  saussurite  occurring  in  the  gab- 
bros of  Lower  Silesia  to  be  like  that  described  by  Oathrein,6  while 
Brogger  mentions  neither  epidote  nor  zoisite,  but  regards  some  mem- 
ber of  the  scapolite  family  as  probably  present  in  the  saussurites  studied 
by  him.7  Paul  Michael  has  recently  investigated  the  saussurite-gabbros 
of  the  Fichtelgebirge  in  Bavaria  and  concludes  that  two  main  types  of 
saussurite  occur  there.  One  of  these  consists  mainly  of  zoisite,  with 
more  or  less  alkaline  feldspar,  and  the  other  is  composed  of  a pale  lime 
alumina  garnet  together  with  serpentine.8 

J.  Lehmann9  and  Lossen10  were  the  first  to  recognize  in  the  saussur- 
itization  of  feldspar  a result  of  dynamic  or  regional  metamorphism — an 
idea  which  Rosenbusch  has  lately  more  clearly  developed  and  elabo- 

1 Die  mikroakopische  Beachaffenheit  der  Mineralion  uud  Gesteino.  Leipzig,  1873,  p.  143. 

2 Die  petrographiscli  wichtigen  Mineralien,  1873,  p.  356. 

3 Tscliermak’s  mineral,  u.  petrog.  Mittheil.,  vol.  1,  1878,  p.  247. 

4Zcitsclir.  Kryst.,  vol.  7,  1883,  p.  234. 

6 Die  fossilien-fiihrcnden  krystallinischen  Sckiefer  von  Bergen  in  Norwegen.  German  translation  by 
Baldauf,  1883,  p.  40. 

6Beitriige  znr  Kenntniss  der  Gabbros,  Amphibolite  und  Serpentino des  nieder-sclilesisclien  Gebirgos. 
Inaug.-Disser.,  188 1,  pp.  7,20. 

7NytMag.  for  Xaturvidouakaberne,  vol.  28,  1884,  p.  253. 

8Nones  Jahrbucb  fur  Mineral.,  1888,  vol.  1,  pp.  36-41. 

9Untersuchungen  iiber  die  Eutstehuug  der  altkrystallinischen  Scbieforgestoinc,  etc.  Bonn,  1884, 

pp.  197,  199. 

,0Jahrbuch  k.  preuss.  geol.  Laudesanstalt  fiir p. 


60 


GREENSTONE  SCHIST  AREAS  OF  MICHIGAN. 


[bull.  62. 


rated.1  This  last-named  authority  shows  that  the  new  mineral  devel- 
oped in  the  feldspar  is  by  no  means  always  of  necessity  zoisite  or  epi- 
dote.  It  may  also  be  garnet,  or  a miueral  of  the  scapolite  family.  He 
remarks:2 

The  sura  total  of  these  new  products,  which  are  certainly  not  produced  by  normal 
weathering,  but  are  due  to  a raetamorphic  process,  we  designate  as  the  saussuritiza- 
tion  of  feldspar.3 

Michel-Levy  was  the  first  to  show  that  the  so  called  “ spotted-gab- 
bro  (gefleckter  Gabbro)  of  Brogger  and  Reusch  was  a mixture  of  arn- 
phibole  and  wernerite  ;4 *  and  Sjogren  has  since  demonstrated  that  the 
latter  mineral  is  secondary  to  feldspar,  and  the  first  to  pyroxene. 
Fouque  and  Michel-Levy  tried  the  interesting  experiment  of  fusing  this 
rock,  and  obtained  therefrom  an  aggregate  of  pyroxene  and  labradorite.6 

Formation  of  the  Albite  Mosaic. — Analogous  and  closely  related  to 
the  saussuritization  of  feldspar  are  cases  where,  in  the  process  of  its 
alteration  by  metamorphism,  the  lime  is  more  or  less  completely  re- 
moved or  crystallized  as  cal  cite,  instead  of  forming  a calcium  silicate. 
In  such  instances  the  alkaline  portion  of  the  plagioclase  molecule  crys- 
tallizes in  the  form  of  a finely  granular  aggregate,  or  mosaic  of  limpid 
grains  (albite).  These  may  be  wholly  devoid  of  twinning  lamellae  and 
often  closely  resemble  quartz,  with  which  they  are  not  infrequently 
associated.  Of  course  such  mosaics  are  connected  by  every  stage  of 
transition  with  saussurite,  according  as  more  or  less  of  the  lime  has  re- 
mained as  a calcium  silicate  (zoisite  or  epidote). 

Such  a granulation  of  the  feldspar  substance  has  already  been 
alluded  to  under  the  head  of  mierostructural  metamorphism;  but,  inas- 
much as  a complete  solution  and  recrystallization  of  clear  feldspar  sub- 
stance often  takes  place,  it  belongs  quite  as  much  to  this  division  of  the 
subject.  The  geological  significance  of  this  method  of  feldspar  altera- 
tion, especially  in  certain  basic  eruptive  rocks  like  diabase,  has  been  most 
persistently  emphasized  by  Lossen.  He  has  shown  how  it  may  result 
in  the  total  obliteration  of  the  original  and  characteristic  rock-struct- 
ure, and  how,  therefore,  it  may  prove  most  misleading,  unless  its  nat- 
ure and  origin  are  clearly  understood.7  J.  Lehmann,9  Teal l,8  and  others 
have  also  observed  and  commented  on  such  a secondary  feldspar 
mosaic. 

Sericitization. — The  soft,  unctuous  mineral  characteristic  of  so  many 
slates  and  schists  was  formerly  regarded  as  talc.  This  gave  rise  to  the 

‘Mikros.  Physiog.,2d  eel.,  vol.  2,  1886,  p.  164. 

2 Ibid.,  p.  137. 

3 “Die  Gesammtheit  dieser  Neubildungen,  die  sicherkeine  Art  der  normaler  Vorwitterung,  sond6rn 
ein  metamorpher  Vorgang  ist,  bezeicknet  man  als  die  Saussuritisirung  des  Feldspatha.” 

4 Bull.  Soc.  Mineral,  de  France,  vol.  1,  1878,  pp.  43,  79. 

fiGeol.  Foreningena Stockholm  Fdrbandl.,  vol.  6,  1883,  p.  447  (Neues  Jahrbuckfiir  Mineral.,  1884,  vol. 
1,  referate  p.  81). 

6 Bull.  Soc.  Mineral,  de  Franco,  vol  2,  1879,  p.  105. 

7Jalirbuck  preuss.  geol.  Landesanstalt  fur  1883,  p.  G40  PI.  29 ; ibid.,  1884,  pp.  525-530,  PI.  xxix,  Figs. 
2 and  4. 

8Uutcrsuchungcn  iiber  die  Entstekung  der  altkrystalliniscken  Scbicfergeatoine,  etc.,  1884,  p.  207. 

9Quart.  Jour.  Geol.  Soc.  London,  vol.  41,  1885,  p.  139. 


WILLIAMS.] 


SERICITIZATION. 


61 


common  designation  “soapstone”  or  “talcose  slates,”  which  was  used 
very  early  in  America  by  Amos  Eaton.1  As  early  as  1819,  however, 
Prof.  Chester  Dewey,  of  Williams  College,  made  the  statement  that  he 
was  able  to  detect  very  little  magnesia  in  the  specimens  which,  he  ex- 
amined, while  alumina  was  abundant.  He  therefore  preferred  to  call 
these  rocks  micaceous  slates.2 

In  Europe,  slates  of  this  kind  were  first  studied  from  the  Taunus, 
where  they  were  usually  regarded  astalcose  until  1847,  when  Sandber- 
ger  made  the  same  discover  that  Dewey  had  made  with  regard  to  the 
American  rocks.3  List  subsequently  studied  more  carefully  this  mica- 
ceous constituent  of  the  Taunus  schists,  and  named  it,  on  account 
of  its  silky  luster,  u Sericite.”4  Scharff  attacked  the  conclusions  of  List 
and  considered  sericite  to  be  only  a mixture,5  while  Lossen  vigorously 
defended  the  individuality  of  the  mineral.6 

The  sericite  was  soon  identified  by  many  investigators  in  the  rocks 
of  many  regions.7  Prof.  Dana  united  it  with  the  species  margaro- 
dite  and  damourite  in  the  group  of  hydro-micas  and  called  this  class 
of  slates  the  hydro-mica  slates.  Of  these  so-called  hydro-micas  Prof. 
Dana  says : 

The  following  species  [margarodite,  damourite,  paropliite,  sericite,  sericite  schist, 
groppite,  enphyllite,  cookeite,  voigtite,  roscoelite,]  are  mica-like  in  cleavage  and  as- 
pect, but  talc-like  in  wanting  elasticity,  in  greasy  feel,  and  in  pearly  luster.  They 
are  sometimes  brittle.  Common  mica,  muscovite,  readily  becomes  hydrated  on  ex- 
posure ; but  hydrous  micas  are  not  all  a result  of  alteration.  Hydro-mica  schists 
form  extensive  rock-formations,  equal  to  those  of  the  ordinary  mica-schists.8 

In  1880  Laspeyres  made  a very  thorough  examination  of  sericite 
and  showed  conclusively  its  identity  with  muscovite.9  It  differs  from 
the  ordinary  form  of  this  species  only  in  its  compact  structure  and  in 
its  geological  significance;  but,  since  both  of  these  are  characteristics, 
there  is  a decided  advantage  in  retaining  the  name  sericite,  especially 
in  petrography,  to  designate  a peculiar  form  and  occurrence  of  musco- 
vite. 

The  alteration  of  orthoclase  into  kaolin  or  clay  was  very  early  known.10 
The  corresponding  change  of  the  same  feldspar  into  mica,  was  first  ob- 
served by  Haidinger  in  1841, 11  but  was  subsequently  found  to  be  not 

I Index  to  the  Geology  of  the  Northern  States,  pp.  147, 174,  28G. 

* Am.  Jour.  Sci.  1st  series,  vol.  1, 1810,  p.  310.  Thus  the  discovery,  usually  attributed  to  Sandberger, 
was  anticipated  in  America  by  twenty-eight  years.  Cf.  Dana's  Manual  of  Geology,  3d  ed.,  p.  72. 

3 Uebcrsicht  d.  geol.  Vorhaltnisso  d.  Horzogth.  Nassau, 1847,  p.  94. 

•*Jahrb.  d.  Vereinsf.  Naturkundo  im  Horxogth.  Nassau,  vol.  G,  1850,  p.  126;  vol.  7,  1851,  p.  266;  vol. 
8,  1852,  p.  128;  Annalen  Chem.  und  Pharni.,  vol.  81,  1852,  p.  181. 

6Neues  Jabrbucli  fur  Mineral.,  18C8,  p.  309  ; ibid.,  1874,  p.  271. 

6Zeitschr.  Deutseh.  mineral,  geol.  Geasell.,  vol.  19,  1867,  p.  509;  vol.  21, 1869,  p.  281. 

7e.  g.,  by  Pichler  in  the  Tyrol.  Neues  Jahrhueh  fur  Mineral.,  1871,  p.56 ; by  Tornebohm  in  Sweden, 
Neues  Jahtbnch  fur  Mineral.,  1874,  p.  141 ; by  von  Laaaulx  in  the  Ardennes;  by  Credner  in  Saxony 
and  by  Wicbmanu  in  the  Lake  Superior  rocks. 

8 Manual  of  Mineralogy  and  Petrography.  4th  ed.  New  Vork,  1887,  p.  335. 

9Zeitschr.  Kryst.,  vol.  4,  1880,  pp.  244-256. 

10  Blum  : Psetidomorphosen  d.  Mineralreichea,  1843,  p.  72. 

II  Abli.  d.  k.  bblim.  Geaell.  d.  Wisaunachaft,  1841,  p.  4.  Bluui:  Paeudomorphosen,  Nuchtr.,  1, 1847, 

p.  25. 


62 


GREENSTONE  SCHIST  AREAS  OF  MICHIGAN. 


{bull.  62. 


uncommon.  Since  rocks  have  been  studied  with  the  microscope,  the 
change  of  potash  feldspar  to  muscovite  or  sericite  has  been  found  to 
possess  a wide  significance,  especially  in  dynamic  metamorphism. 

There  seems  every  reason  to  believe  that  sericite  always  originates 
from  potash  feldspar  and  not  from  other  micas.  Its  constant  and  very 
intimate  association  with  quartz  shows,  as  first  pointed  out  by  Las- 
peyres,1  that  it  was  derived  from  an  acid  silicate. 

Any  rocks,  therefore,  whether  sedimentary  or  massive,  which  con- 
tain orthoclase,  may  give  rise  to  sericite ; but  its  formation,  in  any  case- 
would  seem  to  require  the  action  of  some  great  dynamic  force.  The 
close  relation  between  dislocation  and  mica  formation,  so  clearly  illus, 
trattd  by  J.  Lehmann,2  is  in  an  eminent  degree  applicable  to  sericite. 
It  is  now  a well  known  and  oft-recorded  fact  that  in  any  rock  mass, 
where  the  strains  and  stresses  have  been  the  most  intense,  there  the 
micaceous  minerals  are  most  abundant ; and  if  the  rocks  are  orthoclas- 
tic  these  will  be  largely  sericite.  Sericitization  is  therefore  a phenome- 
non of  dynamic  metamorphism.  It  is  in  a way,  as  Lehmann  says,  a 
retrogressive  metamorphic  process,  since  feldspar  is  by  it  not  formed, 
but  destroyed.  It  is  also  the  most  extreme  manifestation  of  dynamic 
action  in  orthoclase  rocks  and  may  produce  the  same  result — a sericite 
schist — from  a clastic  arkose  on  the  one  hand,  and  from  a massive  gran- 
ite or  quartz-porphyry  on  the  other.3 

In  an  admirable  paper  on  the  paragenesis  of  certain  ore  deposits,  A. 
von  Groddeck  has  shown  that  the  rocks,  heretofore  considered  as  tal- 
cose,  which  occur  near  Holzappel  and  Werlau  on  the  Bhine,  at  Mitter- 
berg  in  Salzburg  and  at  Agordo  in  the  Venetian  Alps,  are  iu  reality 
sericite  schists.  These  he  considers  to  represent  the  extreme  phase  of 
metamorphism,  in  some  cases  of  an  eruptive  rock  (diabase),  and  in  other 
% cases  of  a normal  clay  state  or  graywacke.4  It  seems  most  probable 
that  these  rocks  owe  their  origin  to  dynamic  agencies,  with  which  the 
deposition  of  the  ore  also  stands  in  close  relationship. 

The  alteration  of  the  feldspathic  groundmass  of  quartz  porphyries 
to  muscovite  or  sericite,  especially  where  these  have  been  rendered 
schistose  by  pressure,  is  now  well  known.  In  this  way  porphyroids 
may  be  derived  from  massive  eruptive  rocks.  In  the  more  massive 
quartz  porphyries  studied  by  0.  Schmidt  from  the  central  Alps  (Wiud- 
gallen),  sericite  is  met  with  as  an  occasional  pseudomorph  after  the 
feldspar,  but  in  the  schistose  porphyries  derived  from  the  latter  by  pres- 
sure and  stretching,  this  mineral  is  much  more  abundant ; so  abundant, 
indeed,  as,  in  some  instances,  to  make  up,  along  with  quartz,  the  whole 
mass  of  the  rock.5 6 

‘Zeitschr.  Kryst.,  vol.  4, 1880,  p.  — . 

2Unter8uc1iungen  iiber  die  Entstehung  der  altkrystallinisclien  Schiefergestoine.  Bonn,  1884.  Cap. 
IX.  Druckscliieferung  und  Glimmerbildung,  p.  136. 

•Ibid.,  p.101. 

4Zur  Kenntniss  ciniger  Sericitgestoine,  -welch©  neben  undin  Erzlagerstatten  auftreten.  Neues 

Jahrbuch  fiir  Mineral.,  Beilage-Band  2, 1883,  pp.  72-138. 

6Neucs  Jahrbucb  fiir  Mineral.,  Boilage-Band  4, 1886,  p.  428. 


WILLIAMS.] 


LEUCOXENE. 


63 


Alterations  of  titanic  iron . — The  element  titanium  exists  in  unaltered 
diabases  almost  exclusively  in  combination  with  iron  as  ilmenite  or  as 
titaniferous  magnetite.  In  the  processes  of  metamorphism,  however, 
various  other  titanium  compounds  are  formed.  The  most  common  phase 
of  this  change  consists  in  the  development  of  a gray  rim  around  the 
the  ilmenite  grains.  This  substance  is  also  often  seen  along  the  rhom- 
bohedral  cleavage  cracks  of  the  ilmenite,  giving  rise  to  the  well  known 
gridiron  structure  so  often  figured.1  There  can  be  no  doubt  that  this 
gray  material  is  an  alteration  product  of  the  ilmenite,  although  Giimbel, 
who  gave  it  its  name,  leucoxene , regarded  it  as  a parallel  growth  of 
another  mineral.2  Much  difference  of  opinion  formerly  prevailed  in 
regard  to  the  chemical  nature  of  the  leucoxene.  Zirkel  at  first  regarded 
it  as  iron  carbonate,3  Cohen  as  titanic  oxide,4  Rosen busch  as  anatase.5 
Giimbel  regarded  it  as  probably  a titanosilicate,  while  both  Fouque6 
and  Michel-Levy7  thought  that  it  was  a form  of  sphene.  The  identity 
of  both  leucoxene  and  titano-morphite  (another  similar  substance 
described  by  von  Lasaulx  around  the  rutile  of  an  amphibolite  from 
Lampersdorf  in  Silesia)8  with  titanite  or  sphene  was  first  conclusively 
proved  by  A.  Cathrein  in  1882.9 

The  freqnent  passage  of  the  dull  gray  leucoxene  rim  into  clearly  de- 
fined aggregates  and  crystals  of  sphene  is  mentioned  by  Cathrein,10  and 
the  origin  of  sphene  by  the  alteration  of  ilmenite  is  also  described  by 
W.  C.  Brogger.11  Fine  examples  of  this  origin  for  sphene  are  also 
described  and  figured  in  the  sequel. 

Anatase  has  been  described  as  an  alteration  product  of  ilmenite,  by 
Differ.12 

The  rutile  needles  frequently  seen  about  ilmenite,  either  with  or 
without  leucoxene,  are  regarded  by  Cathrein  as  an  original  intergrowth 
of  this  mineral  with  the  ilmenite.13  Further  reference  will  be  made 
hereafter  to  needles  of  this  character  occurring  in  some  of  the  Menom- 
inee greenstones. 

*Cf.  Valloo'do  la  Poussin  et  Renard:  Roclies  plutoniennes  de  la  Belgique,  etc.,  1874,  PI.  VI,  Figs  31 

and  32. 

2 Palseolithische  Eruptivgesteine  des  Fichtelgebriges,  Munich,  1874,  p.  35. 

* Mikroskopischo  Beschaffenheit  d.  Min.  u.  Gest.,  1873,  p.  409. 

4Erliiaternde  Bemerkungen  z.  d.  Routenkartc,  etc.,  1875,  p.  55. 

5Mikros.  Physiog.,  1st  ed.,  vol.  2,  1877,  p.  336. 

e Cours  do  College  do  France,  1877. 

7 Bull.  Soc.  G6ol.  France,  3d  series,  vol.  6,  1878,  p.  163. 

"Neues  Jahrbuch  fur  Mineral , 1879,  p.568. 

*Zeitschr.  Kryst.  u.  Min.,  vol.  6, 1882,  p.  244. 

10  Ibid. 

11  Nyt  Mag.  for  Naturvidenskaborne,  vol.  27, 1884,  p.  359. 

12Neues  Jahrbuch  fiir  Mineral.,  1883,  vol.  1,  p,  193, 

>*  Zeitschr.  Kryst.  u.  Min.,  vol.  6,  p.  256. 


CHAPTER  II. 


GREENSTONE  BELTS  OF  THE  MENOMINEE  IRON  DISTRICT. 

INTRODUCTORY  AND  HISTORICAL. 

The  exact  geographical  position  of  the  two  greenstone-schist  areas 
of  the  Menominee  region  are  fully  indicated  in  the  explanatory  and 
historical  note  by  Prof.  Irving  at  the  beginning  of  this  memoir 
and  upon  the  accompanying  geological  map  of  this  district.  (PI.  II). 
The  same  note  explains  and  discusses  the  different  views  which  have 
been  held  by  various  geologists  in  regard  to  the  stratigraphical  position 
of  these  greenstone  schists  in  the  general  succession  of  the  stratiform 
rocks  of  the  Menominee  region. 

A brief  mention  of  the  opinions  which  have  already  been  published 
regarding  the  petrographical  character  of  these  greenstone  schists 
is,  however,  desirable. 

The  first  attempt  to  describe  the  Menominee  greenstones  and  green- 
stone schists  lithologically  was  made  by  Hermann  Credner  in  i860, 
from  observations  collected  while  he  was  acting  as  assistant  to  Prof. 
Pumpelly  on  a survey  for  the  Portage  Lake  and  Lake  Superior  Ship 
Canal,  during  the  years  1867- C8.1  In  his  first  paper  entitled  Die  vorsi- 
lurischen  Gebilde  der  oberen  Halbinsel  von  Michigan  in  Nord-Amerika ,2 
Credner  gives  a section  of  the  strata  of  the  Menominee  Iron  Region, 
commencing  with  the  oldest  member,  from  which  the  following  is  abbre- 


viated : 

Feet. 

a.  Quartzite 8,000 

1).  Crystalline  dolomitic  limestone 3,500 

c.  Red  Iron  ore 600-1,000 

d.  Chlorite  schist 1, 000-1, 500 

e.  Clay  slate 8,500 

/.  Chlorite  schist  with  diorite 1,200-1,400 

g,  h,  i,  k.  Talc  schist 150 

l.  Dioritic  series „ 2,300 

m.  Talcose  clay  slate 1,500 


The  members  / and  l are  evidently  parts  of  the  same  formation,  in 
which  the  beds  g , h , i,  and  h are  interstratified.  In  his  description  of 
/,  Credner  says : 

In  the  upper  horizon  of  this  series  there  occur  beds  of  fine  and  coarse  grained 
diorite  and  aphanite,  varying  in  thickness  from  ten  feet  to  several  hundred.  These 


64 


1 See  Geology  of  Michigan,  vol.  1, 1873,  p.  157,  note. 

2Zeitachr.  Deutsch.  geol.  Ge3cll.,  vol.  21, 1869,  pp.  516-554. 


WILLIAMS.  ] 


WORK  OF  CREDNER  AND  BROOKS. 


65 


rocks  consist  mainly  of  dark  green  hornblende  and  white  or  pale  green  oligoclase, 
with  which  granular  or  scaly  chlorite  is  often  associated.  Crystals  of  pyrite  and  mag- 
netite are  also  frequent.  Indications  of  a lamellar  parting  are  frequent,  while  rect- 
angular jointing  is  rare.1 

In  the  same  article,  in  speaking  of  the  member  £,  the  author  says  :2 

Dioritic  series  2,300  feet  in  thickness.  Mainly  a fine  grained  or  aphanitic,  rarely 
a coarsely  crystalline  aggregate  of  the  constituents  of  diorite.  All  contain  crystals 
of  pyrite  ; the  aphanite  contains  veins  of  calcite  and  quartz.3 

In  a second,  article  entitled  Ueber  nor damer iJcanische  tSchieferporphy- 
roide , which  also  deals  with  certain  rocks  exposed  on  the  Meuominee 
River,4  Oredner  unites  his  beds  / and  l as  “chlorite  schist  alternating 
with  intercalated  diabase  ; 77  while  his  g , h,  i,  and  Jc  are  described  as  a 
series  of  “ porphyroid-schists, 77  300  feet  in  thickness,  between  two  beds 
of  diabase. 

In  the  year  1869  the  geological  survey  of  Michigan  was  inaugurated 
with  the  iron-bearing  formations  of  the  Upper  Peninsula,  in  charge  of 
Maj.  T.  B.  Brooks.  The  results  of  his  labors  appeared  in  1873, 5 accom- 
panied by  two  appendices,  containing  special  petrographical  descrip- 
tions of  the  rocks  collected  by  Julien,6  and  Wright.7  Several  of  the 
Menominee  greenstones,  both  massive  and  schistose,  come  within  these 
descriptions,  but  the  descriptions  are  for  the  most  part  vague;  as,  for 
instance  “diorite/  “dioritic  schist/  “ porphyritic  diorite/  etc. 

In  1874  Major  Brooks  continued  his  studies  of  the  Menominee  region 
under  the  auspices  of  the  Wisconsin  Geological  Survey.  The  results 
of  this  work  appeared  in  1879 8 and  contained  much  more  elaborate 
and  accurate  determinations  of  the  greenstones  and  greenstone  schists. 
Major  Brooks  gives  a diagram9  to  illustrate  his  general  views  of  the 
observed  transitions  of  greenstones  (believed  to  be  mostly  metamor- 
phosed sediments)  into  related  rocks.  Dr.  Wichmanu,  who  furnished 
the  systematic  petrographical  descriptions  of  these  rocks  iu  Brooks’s 
report,10  however,  regarded  these  rocks  as  for  the  most  part  eruptive 
and  to  a large  extent  as  derived  from  diabase.  Special  reference  will 
be  made  to  the  descriptions  of  Wichmann  and  others  who  have  worked 

1 Zeitschr.  Deutsch.  geol.  Gesell.,  vol.  21,  1869,  p.  528. 

7 Im  oberen  Horizonte  dieser  Schichtenreihe  treten  von  10  bis  mehrere  hundert  Fuss  macbtige  Einla- 
gerungen  von  fein-  bis  grobkoruigem  Diorit  sowie  von  Aphanit  auf.  Sie  beetehen  vorwaltend  aus 
dunkelgriiner  Hornblende  und  weissem  oder  kellgriinem  Oligoklas,  wozu  sich  an  mancben  Pnnkten 
viel  kornig-scliuppiger  Chlorit  gesellt.  Einsprenglinge  von  Schwefelkies  und  Magneteisenstein  sind 
iu  ihnen  haufig.  Andeutung  von  plattenformiger  Absonderung  ist  gewohnlich,  quarderformige  Ab- 
aonderung  selten. 

* Ibid.,  p.  529. 

4 Dioritische  Gesteinsreihe  von  2,300'  Macbtigkeit.  Vorwaltend  ein  feinkorniges  oder  aplianitiscbes, 
seltener  eiu  grobkrystalliniscbes  Gemenge  der  Bestandtbeile  des  Diorites,  alle  mit  Schwefelkies  ein 
ein  sprenglingen,  die  Aphanite  ink;  Schuiiren  von  Kalkspath  und  Quarz. 

‘ 6Neues  Jabrbuch  fur  Mineral.,  1870,  pp.  970-984. 

‘Geol.  Survey  Michigan,  vol.  1,  Upper  Peninsula.  Part  I.  Iron-bearing  rock,  by  T.  B.  Brooks.  1873. 

7 Ibid.,  vol.  2,  1873.  Appendix  A,  Lithological  descriptions,  etc.,  of  259  specimens  of  the  Huronian 
and  Laurentian  of  the  Upper  Peninsula,  by  A.  A.  Julien,  pp.  1-197. 

*Ibid.,  vol.  2,  1873.  Appendix  C.  Microscopic  determinations  and  descriptions  of  78  specimens  of, 
Huronian  rocks  and  ores,  by  O.  E.  Wright,  pp.  213-231. 

#Geol.  Wisconsin,  Vol.  3,  1873-1879.  The  Geology  of  the  Menominee  Iron  Region,  Oconto  County, 
by  T.  B.  Brooks,  pp.  429-663.  Ibid  , Geol.  Menominee  Region  by  C.  E.  Wright,  pp.  065-741, 

,0Ibid.,  519.  "Ibid.,  pp.  000-656, 

Bull.  62- — 5. 


66 


GREENSTONE  SCHIST  AREAS  OF  MICHIGAN. 


[BULL.  62. 


upon  the  petrography  of  the  Menominee  greenstones  in  the  course  of 
the  following  chapters  of  this  work. 

All  observers  seem  to  be  agreed  that  the  association  of  the  massive 
greenstones  with  those  which  are  more  or  less  perfectly  schistose  is  an 
extremely  intimate  one.  Even  Major  Brooks,  in  spite  of  his  idea  that 
most  of  the  greenstones  are  altered  sediments,  is  constantly  suggesting 
the  possibility  of  a mechanical  origin  for  the  intercalated  schistose  lay- 
ers. He  says 1 of  the  Twin  Falls  exposure : 

This  slaty  material  may  be  simply  a compacted  form  of  the  pulverized  greenstone 
produced  at  the  time  of  Assuring. 

Again,2  in  speaking  of  the  Commonwealth  aud  Eagle  Mine  rocks: 

It  will  be  observed  that  these  rocks  have  some  resemblance  to  aa,  but  it  is  be- 
lieved that  they  are  associated  schistose  and  altered  varieties  of  the  great  greenstone 
bed  XVIIL  so  extensively  developed  to  the  north  and  east. 

He  says3  also: 

An  unevenly  splitting,  gray-green  schist  associated  with  greenstones  and  appar- 
ently derived  from  them  by  alteration  of  the  amphibole,  is  included  in  this  family 
(chlorite  schist],  although  its  origin  and  associations  are  widely  different  from  the 
above. 

Again : 4 

One  of  the  largest,  most  generally  distributed,  and  at  the  same  time,  obscure  va- 
rieties embraces  those  chloritic  rocks  that  are  associated  with  greenstones. 

Dr.  C.  Kominger,  in  his  Report  on  the  Geology  of  the  Menominee 
Iron  Region,5  is  equally  impressed  with  the  close  association  of  the 
massive  aud  schistose  varieties  of  the  greenstones.  Like  Brooks,  he 
regards  them  as  of  sedimentary  origin,  and  thinks  that  the  massive 
portions  are  the  result  of  extreme  metamorphism,  having  recrystallized 
from  a partially  fused  state. 

There  seem  to  be  only  three  different  ways  of  explaining  the  facts  as 
they  are  plainly  and  abundantly  manifested  at  each  of  the  several  points 
examined  on  the  Menominee  River. 

We  may  suppose,  as  did  Foster  and  Whitney,  Whittlesey  and  Cred- 
ner,  that  the  schistose  portions  of  the  rocks  exposed  at  these  several 
points  are  more  or  less  perfectly  metamorphosed  sedimentary  material, 
while  the  more  massive  portions  represent  intercalated  beds  of  eruptive 
origin. 

We  may  imagine,  on  the  other  hand,  as  did  Rominger  and  Brooks, 
that  all  of  these  rocks,  including  the  most  schistose  aud  the  most  mas- 
sive phases,  are  probably  altered  sedimentaries;  supposing,  with  Romin- 
ger, that  the  more  massive  kinds  are  merely  the  same  sedimentary  mate- 
rial fused  by  the  intensity  of  the  metamorphosing  action  so  as  to  lose  all 
trace  of  the  original  stratification ; or  admitting,  with  Brooks,  the  possi- 
bility, though  great  improbability,  that  some  of  the  more  massive 
phases  like  the  gabbro  of  Sturgeon  Falls,  are  of  eruptive  origin. 

1 Geol.  Wisconsin,  vol.  3,  1873-1879.  The  Geology  of  the  Menominee  Iron  Region,  Ocorets  County,  by 
T.  B.  Brooks,  p.  477. 

2 Ibid.,  p.  484. 

4 Ibid.,  p.  518. 


3 Ibid.,  p.  516. 

fiGool.  Michigan,  vol.  4,  1881,  p.  209. 


WILLIAMS.] 


STURGEON  FALLS  GABBRO. 


67 

Finally,  we  may  imagine  tliat  all  phases  seen  at  these  several  places 
represent  material  of  eruptive  origin  whose  stratiform  structure  is  due 
to  secondary  dynamic  agencies.  This  last  view  has  heretofore  been 
advanced  only  by  Irving,  who,  however,  has  presented  it  very  briefly, 
and  without  descriptions  or  petrographic  proof.1 

It  is  the  aim  of  the  present  portion  of  this  paper  to  set  forth  all  the 
evidence  that  a careful  examination  of  these  rocks  can  furnish  as 
to  which  of  these  three  views  best  explains  their  true  origin  and  mu- 
tual relations.  This  material  will  first  be  presented  in  the  form  of  a 
detailed  description  of  each  of  the  five  localities  selected  for  this  pur- 
pose on  the  Menominee  River  (see  PI.  II).  The  general  results  thus  se- 
cured will  be  summarized,  in  connection  with  those  obtained  elsewhere, 
in  Chap.  VI.  The  Menominee  localities  will  be  treated  of  in  regular 
order,  commencing  with  the  one  farthest  down  the  river,  Sturgeon  Falls. 

STURGEON  FALLS. 

Kinds  of  rock. — This  exposure  is  situated  a short  distance  below  the 
mouth  of  the  Sturgeon  River,  in  Sec.  27,  T.  39  N.,  R.  29  W.,  Michigan.  Its 
general  topography  may  be  seen  from  the  accompanying  map  (PI.  Ill), 
which  is  copied  from  PI.  I,  in  Major  Brooks’s  report  with  double  his  linear 
scale.  Only  the  rocks  exposed  on  the  eastern  or  Michigan  side  of  the 
river  were  examined ; but  those  opposite  could  be  seen  to  be  of  the 
same  character. 

The  barrier  which  here  forms  the  falls  consists  of  two  belts  of  mas- 
sive rock, /and  h , between  which  are  softer  schists,  g.  These  are  also 
intercepted  by  a harder  and  more  massive  band. 

The  massive  rock  is  light  in  color  and  of  a comparatively  coarse  grain. 
It  is  quite  elaborately  described  in  Major  Brooks’s  report,2  and  desig- 
nated on  the  authority  of  Wapler,  Rutley,  and  Pumpelly  as  a gabbro. 
Julieu  also  examined  this  rock,  but. seems  to  have  mistaken  the  diallage 
for  hornblende,  and  the  brown  pleochroic  hornblende  for  biotite.  Rut- 
ley’s  opinion  is  given  with  hesitation.  Pumpelly’s  description  is  brief 
and  accurate.  He  says  :3 

Saussurite-gabbro  (or  hornblende  gabbro) : contains  saussurite,  diallage,  horn- 
blende. Identical  under  the  microscope  with  the  coarser  crystalline  rock  of  Upper 
Quinnesec  Falls. 

This  rock  was  considered  serpentine  by  Foster  and  Whitney4  and 
was  provisionally  named  ‘‘porpbyritic,  speckled  diorite”  by  Brooks, 
who  separated  it  as  his  Bed  XV  of  the  Huronian. 

The  massive  occurrence  at  /is  represented  by  Nos.  11154,  11155,  and 
11162;  that  at  h by  Nos.  11107,  11168,  11169,  and  11170.  Nos.  11156- 
11161,  and  11163-11166  were  collected  from  the  softer  schistose  bauds 
at  g. 

These  rocks  are  particularly  noteworthy  as  being  the  only  ones  dis- 
covered on  the  Menominee  River  which  contained  any  trace  of  pyroxene. 


1 Fifth  Annual  Report  U.  S.  Geol.  Survey,  p.  190.  2 Geol.  Wisconsin,  vol.  3,  pp.  455-563. 

Ibid5 p.  564.  4 Report  on  the  GeoL  Lake  Superior  Land  District  Plate  2,  p.  25. 


68 


GREENSTONE  SCHIST  AREAS  OF  MICHIGAN. 


| BULL.  62. 


We  shall  find  that  they  agree  perfectly  with  Pumpelly’s  description 
above  cited,  the  hornblende  being  in  part  secondary,  and  they  are  hence 
to  be  designated  as  saussurite  gabbro.  The  least  altered  specimens  were 
found  at  li  (Nos.  11167-11170).  The  rock  at /,  although  essentially  the 
same  as  at  h , i$  more  changed  and  somewhat  schistose  along  certain 
bands,  while  some  of  the  specimens  found  at  g were  clearly  once  the 
same  as  the  others,  but  now  represent  a third  and  much  more  advanced 
stage  of  alteration.  I shall  first  describe  these  three  stages  of  the 
undoubted  gabbro,  and  then  trace  their  relation  to  the  intermediate 
schists. 

Saussurite- gabbro  (first  stage). — The  color  of  this  rock  in  the  hand, 
specimen  is  rather  light.  On  a fresh  fracture  it  shows  a finely  mottled 
structure  of  white  and  dark  greenish-gray.  Examined  with  a pocket- 
lens,  the  mottling  is  seen  to  be  due  to  two  minerals.  One  of  these  is 
opaque  white,  sometimes  tinged  with  green,  and  only  rarely  exhibits 
the  glistening  cleavage  surface  of  feldspar.  The  darker  mineral  has  a 
brownish  color  and  almost  a metallic  luster  on  its  cleavage  surface.  It 
is,  however,  always  tinged  with  green  on  account  of  incipient  altera- 
tion. 

No  other  constituents  are  microscopically  visible.  The  structure  of 
the  rock  is  irregularly  granular.  The  grain  is  as  a rule  moderately  fine 
but  is  subject  to  sudden  local  variation  which  develops  comparatively 
coarse- grained  patches  in  the  main  mass. 

Of  this  freshest  type  of  the  gabbro  four  thin  sections  were  studied, 
viz,  11167,  11167a,  11168  and  11170.  All  show  profound  alteration  in 
the  original  constituents,  due  to  dynamic  processes.  These  are,  how- 
ever, most  intense  in  No.  11167,  which  has  been  subjected  to  such  great 
pressure  as  to  present  a transition  form  to  the  second  stage  of  this 
gabbro.  Nos.  11167a,  11168,  and  11170,  are  practically  identical  and 
may  be  described  together. 

Under  the  microscope  this  rock  is  seen  to  be  composed  of  plagioclase, 
almost  wholly  altered  to  a gray  and  opaque  saussurite;  diallage,  of  a 
very  light  gray  color ; hornblende,  partly  original,  partly  secondary,  and 
a little  titanic  iron  (hmenite).  Certain  alteration  products,  like  quartz, 
caicite,  and  a colorless  chlorite,  are  also  present  in  varying  quantity. 

The  feldspar  has  no  crystal  form  of  its  own  (i.  e.,  it  is  allotriomor- 
phous,  in  the  sense  of  Rosenbusch).  It  seems  to  have  crystallized  sim- 
ultaneously with  the  diallage,  or  if  anything  later.  It  is  hardly  ever 
so  unaltered  as  to  present  its  original  twinning-lamellm,  but  when  this 
is  the  case  the  high  extinction  angles  and  brilliant  interference  colors 
observed  indicate  a basic  feldspar.  No  further  determinations  could  be 
made  on  this  mineral  because  of  its  almost  complete  alteration  to  a 
dull  opaque  white  saussurite.  Even  in  the  thinnest  sections  this  sub- 
stance remains  opaque  for  the  lower  powers  of  the  microscope,  being 
composed  of  such  fine  grains  that  it  must  be  highly  magnified  before  it 
can  be  resolved.  Under  higher  powers,  however,  it  is  seen  to  be  made 


U.  S.  GEOLOGICAL  SURVEV 


BULLETIN  NO.  62  PL.  Ill 


THt  l»*kW 
OF  THE 

UHIVERSITT  OF  U-UHOIS 


williams.]  ALBITE  AND  ZOISITE  IN  SAUSSURITE.  69 

up  of  small  zoisite  grains,  embedded  in  a clearer  matrix,  which  is  prob- 
ably albite.1 

This  saussurite  substance  is  traversed  in  all  directions  by  lighter— 
sometimes  quite  clear  aud  transparent— veins,  which  are  composed 
largely  of  secondary  albite.  This  in  at  least  one  instance  (No.  11168) 
shows  the  characteristic  twinning  striation  of  plagioclase  (see  Fig.  4). 
In  other  cases,  however,  these  veins  appear  to  be  composed  of  quartz 
or  chlorite  (see  PI.  VIII,  fig.  1). 


Fig.  4. — Veins  filled  with  secondary  albite  in  Fig.  5.— Zoisite  crystals  in  a coarse  saus- 

the  altered  gabbro  of  Sturgeon  Falls  (Ho.  surite  from  the  altered  gabbro  of  Sturgeon 

11168).  It.-presented  in  polarized  light  in  or-  Falls.  Magnified  180  diameters, 

der  to  show  the  twinning  striae.  Magnified 
350  diameters. 

In  certain  cases,  notably  in  section  No.  11167,  the  saussurite  aggre- 
gate is  coarser  and  the  zoisite  plainly  visible  aud  easily  determinable. 

Fig.*5  shows  characteristic  forms  of  this  mineral.  Its  crystals  are 
always  without  terminal  planes,  but  they  have  a perfectly  developed 
cleavage  parallel  to  their  vertical  axis  and  a cross-jointing.  Between 
crossed  nicols  they  are  seen  to  be  twinned,  sometimes  polysynthetically, 
like  albite.  The  zoisite  is  itself  colorless,  with  a high  index  of  refrac- 
tion, but  a weak  double  refraction ; the  interference  colors  are  therefore 
dull,  either  gray  or  bluish,  and  sometimes  a deep  ultramarine.  The  ex- 
tinction is  parallel  to  the  cleavage  lines. 

One  unusually  large  crystal  of  zoisite,  represented  in  Fig.  6,  exhibits 
all  of  these  characteristics,  and  also,  when  examined  in  converged  polar- 
ized light,  it  gives  a biaxial  interference  figure  with  the  plane  of  the  optic 
axes  perpendicular  to  the  cleavage.  (Fig.  6.) 

1 Zeitschr.  Kryst.  u.  Min.,  vol.  7,  pp.  234-249.  Cathrein,  in  this  article,  calculates  a number  of 
saussurite  analyses  to  show  the  relative  amounts  of  feldspar  and  zoisite  or  epidote  present.  He  seems 
to  think  that  the  feldspar  left  after  subtracting  the  zoisite  gives  the  original  constitution  of  the  min- 
eral before  its  change  to  saussurite,  and  attributes  the  alteration  to  the  addition  ofCaO  aud  A1.203  and 
loss  of  silica  and  alkalies  (p.  243).  Another  hypothesis  would  bo  that  the  original  feldspar  was  much 
more  basic  (i.  e.,  contained  more  CaO,  A1203  and  less  §i02  and  Ha20)  than  the  one  now  forming  the 
matrix  of  the  saussurite,  and  that  this  compound  broke  up  without  material  chemical  change  into  two 
compounds,  one  a more  acid  plagioclase,  like  albite  or  oligoclaso  and  the  other  zoisite,  which  would 
contain  what  CaO  and  superfluous  A1203  was  left  after  the  change.  A similar  separation  of  one  min- 
eral into  two  has  boon  traced  by  Profs.  J.  Brush  and  E.  S.  Dana  in  the  alteration  of  spodumeue  into 
a minute  aggregate  of  eucryptito  and  albite.  (Am.  Jour.  Sci.,  3d  series,  vol.  20,  p.  257  et  seq.,  1880.) 


70 


GREENSTONE  SCHIST  AREAS  OF  MICHIGAN. 


[BULL.  62- 


The  diallage  of  these  rocks  is  quite  colorless  when  seen  in  a thin  sec- 
tion, although  in  the  form  of  powder  it  is  a light  grayish  green.  The 
prismatic  cleavage  is  well  developed,  but  not  as  much  so  as  the  very 
perfect  parting  parallel  to  the  ortkopinacoid,  which  is  the  characteris- 
tic feature  of  diallage  (PI.  VIII,  fig.  1).  The  extinction  angle  was  found 
to  be  as  great  as  35°  in  the  prismatic  zone.  The  plane  of  the  optic 
axes  is  perpendicular  to  the  orthopinaeoidal  parting,  and  a single  axis 
appears  in  such  sections  as  show  a prismatic  angle  of  nearly  90°.  This 
diallage  is  very  sensitive  to  the  action  of  pressure  and  is  frequently 
much  bent  and  twisted.  The  mineral  is  sometimes  separated  along 
cleavage  cracks,  the  interstices  being  filled  with  a colorless,  isotropic 
alteration  product,  which  is  probably  some  variety  of  chlorite.  This 
substance  becomes  much  more  abundant  in  the  more  altered  forms  of 
this  rock  and  will  be  again  mentioned.  The  diallage  is  also  often  trav- 
ersed by  veins  filled  with  clear  quartz. 


Fig.  6. — Large  crystal  of  zoisitein  saussurite 
of  No.  11167.  Altered  gabbro  from  Sturgeon 
Falls.  Magnified  350  diameters. 


Fig.  7. — Border  of  both  compact  and  fibrous 
hornblende  around  diallage  in  the  Sturgeon 
Falls  gabbro  (No.  1167a).  Magnified  180  diame- 
ters. 


The  hornblende  is  an  important  and  constant  constituent  of  the 
Sturgeon  Falls  gabbro.  It  is  for  the  most  part  compact,  and  brown  in 
color,  having  the  usual  pleochroism.  More  rarely  it  is  green,  or  ap- 
parently bleached  to  a lighter  shade  of  brown.  In  a few  instances 
this  latter  process  has  been  carried  so  far  as  to  make  it  quite  colorless. 
The  hornblende  is  in  all  cases  most  intimately  associated  with  the  dial- 
lage. At  times  it  forms  a continuous  border  of  varying  width  around 
the  diallage  crystal,  and  in  other  instances  it  penetrates  the  latter 
mineral  in  irregular  areas  ( see  PI.  VIII.  fig.  1).  In  some  cases  a deli- 
cate fringe  of  minute,  colorless  hornblende  fibers  is  seen  to  lie  on  the 
outer  side  of  the  compact  hornblende  border  and  penetrate  the  saus- 
surite substance  (see  Fig.  7).  This  is  the  same  phenomenon  that  has 
recently  been  described  by  Lossen.1 


1 Studien  an  metamorpbischen  Eruptiv-  uud  Sedimentgesteine,  etc.,  cf.  Jahrbuch  preuss.  geol.  Land- 
esanstalt  fur,  1884,  p.  543,  PI.  xxix,  fig.  2.  (Cf.  Van  Hise:  Am.  Jour.  Sci.,  3d  series,  vol.  33,  1887,  pp 
385  et  seq. 


WILLIAMS.] 


HORNBLENDE  AND  CHLORITE  IN  GABBRO. 


71 


It  is  impossible  to  say  with  certainty  what  the  origin  of  the  com- 
pact brown  hornblende  is.  It  may  be  an  original  product  of  crystal- 
lization in  the  magma,  but  its  mode  of  occurrence  and  its  general 
character  indicate  that  it  is  probably  of  secondary  origin,  having 
originated  by  paramorphism  of  the  diallage,  as  has  been  shown  by  my- 
self1 and  by  Lossen2  to  be  sometimes  the  case. 

No  other  constituents  are  important  in  this  rock.  Iron  in  any  form 
seems  to  be  quite  rare  in  it.  Occasional  cloudy  grains,  resembling 
leucoxene,  may  represent  some  original  ilmenite,  while  minute  crystals 
of  pyrite  are  still  rarer. 

The  structure  of  the  rock  seems  to  be  irregularly  granular ; none  of 
the  components  being  in  any  degree  idiomorphic.  Frequent  and 
abrupt  changes  in  the  coarseness  of  the  grain  are  observable. 

All  specimens  show  the  action  of  dynamic  forces  which  have  more  or 
less  profoundly  affected  the  different  constituents.  These  effects  are 
particularly  noticeable  in  slide  No.  11167.  Here  the  rock  seems  in 
places  to  have  been  crushed  and  a mosaic  of  the  component  minerals 
to  have  been  formed.  Hornblende,  generally  colorless,  is  unusually 
abundant.  Colorless  chlorite  and  zoisite  are  also  developed,  and  all  are 
mixed  indiscriminately.  In  one  part  of  the  section  a vein  is  s*  en  to 
traverse  the  rock.  This  is  filled  with  limpid  quartz  in  long,  wedge- 
shaped  areas,  which  extend  from  one  side  of  the  small  fissure  to  the 
other.  This  quartz  is  traversed  by 
long,  colorless  fibers  of  the  greatest 
delicacy,  and  it  also  contains  a good 
deal  of  the  colorless  chlorite,  both  in 
solid  masses  and  in  those  peculiar 
vermicular  groups  to  which  Volger 
has  given  the  name  helminth.  These 
curious  groups,  which  resemble  piles 
of  little  coins,  are  sometimes  straight, 
sometimes  curved.  They  are  so  mi- 
nute as  to  be  visible  only  with  a high 
magnifying  power.  Fig.  8 represents 
them  as  they  appear  when  magnified 
350  diameters.  Exactly  the  same  min- 
eral has  been  described  in  the  sec- 
ondary quartz  of  diabase  by  Molil,3  von  Lasaulx 
in  that  of  schalstein  and  syenite  by  Hussak.6 

Samsurite  gabbro  [second  stage). — Representatives  of  this  type  are 
found  at  the  lower  end  of  the  falls,  at  / on  Major  Brooks’s  map,  and 

'Am.  Jour.  Sci.  3d  series,  vol.  28,  Oct.,  1884,  p.  262. 

2cf.  J ahrbuch  preass.  geol.  Landesanstalt  fur  1883,  p.  632. 

3 if  cues  J ahrbuch  fur  Mineral.,  1875,  p.  716. 

4 Verh.  d.  naturh.  Vereins  d.  preuss  Rlieinl.  u.  Westf.,  1878,  p.  216. 

6 Inaugural-Disseitation.  Bonn,  1884,  p.  22. 

6 Tschermak’s  mineral,  u.  potrog.  Mittheil.,  vol.  1,  1878,  p.  275. 


Pig.  8. — Vermicular  chlorite  (helminth)  in 
quartz.  Vein  in  altered  gabbro,  Sturgeon 
Palls. 

and  Schenck  f and 


72 


GREENSTONE  SCHIST  AREAS  OF  MICHIGAN. 


[BULL  *62. 


at  his  e , at  the  lower  end  of  the  basin  below  the  falls.  Nos.  11153  and 
11154,  from  these  two  localities,  are  identical  in  mineral  composition 
with  the  rocks  of  the  first  type  above  described.  They  are  of  a dirty 
greenish  gray  color  and  indications  of  a schistose  structure  have  already 
begun  to  appear  in  them.  Under  the  microscope  they  disclose  the 
same  constituent  minerals  as  the  rocks  of  the  first  type;  nor  are  these 
minerals  much  more  altered,  but  they  show  the  effects  of  a profound 
mechanical  action.  The  feldspar  is  remarkably  fresh  and  its  twinning 
lamellse  are  quite  distinct,  but  it  is  everywhere  crushed,  broken,  and 
faulted.  The  crystals  are  often  plainly  seen  to  be  separated  into  a 
number  of  fragments  which  are  removed  a considerable  distance  from 
one  another.  Frequently  a fine  grained  mosaic  has  been  formed  by 
the  crushing  of  the  larger  feldspar  crystals.  In  other  cases  (especially 
in  section  11154)  the  feldspar  is  not  so  much  broken,  but  it  is  altered 
around  its  edge  to  an  opaque,  gray  saussuritic  mass,  while  its  interior  is 
hardly  changed.  (See  PI.  VIII,  fig.  2).  The  diallage  is  more  altered 
than  in  the  rocks  last  described,  although  it  can  still  be  seen  to  belong 
to  the  same  species.  The  crystals  are  very  much  bent  and  twisted  and 
frequently  so  changed  to  the  light-colored  chlorite  that  only  a few 
minute  remnants  of  the  brightly  polarizing  mineral  remain  m this 
nearly  isotropic  base.  (See  PI.  VIII,  fig.  2.)  Fibrous  hornblende  now 
becomes  more  abundant  than  the  compact,  and  leucoxene  patches  are 
seen  at  intervals. 

Nos.  11162,  from  the  upper  part  of  the  point  /,  and  11172  from  above 
the  falls  at  n , present  interesting  varieties  of  this  rock.  They  do  not 
show  the  effects  of  crushing  to  such  a degree  as  do  those  just  described. 
Indeed  the  original  structure  of  the  rock  seems  well  preserved,  although 
the  feldspar  is  almost  completely  changed  to  a fine  grained,  nearly 
opaque  saussurite,  and  every  trace  of  the  pyroxene  (diallage)  has  dis- 
appeared. A pale  green,  fibrous  hornblende  occupies  the  place  of  this 
mineral,  and  there  seems  to  be  every  reason  for  regarding  it  as  derived 
from  the  diallage ; although  in  No.  11172  the  abundant  remains  of  a 
compact,  brown  hornblende,  evidently  in  the  process  of  changing  to 
the  fibrous  modification,  suggests  the  possibility  of  this  mineral  having 
been  the  original  bisilicate  constituent.  Still  there  is  no  warrant  for 
assuming  that  what  is  essentially  a diallage  rockmass  was  locally  de- 
veloped as  a hornblendic  rock ; and  it  may  be  that  this  is  an  instance 
of  a remarkable  passage  of  a pyroxene  through  a compact  into  a fibrous 
hornblende , for  which  we  shall  find  much  evidence  in  the  studies  that 
follow. 

Saussurite  gabbro  ( third  stage). — As  has  been  already  remarked  and  as 
may  be  seen  on  the  map  of  Sturgeon  Falls  (PI.  Ill),  there  is,  between 
the  two  points  of  the  more  massive  rock,  li  and /,  an  area  </,  composed 
of  softer  schists.  These  are  easily  eroded  and  have  thus  occasioned  the 
small  bay.  The  passage  from  the  fresh  and  massive  gabbro  at  h into 


WILLIAMS.  ] 


EXTREMELY  ALTERED  GABBRO. 


73 


these  schists  seems  to  be  a gradual  one.  Aloug  the  lower  side  of  h 
there  are  rocks  which  are  without  doubt  essentially  the  same  as  those 
above  described  from  this  point  but  which  have  been  profoundly  altered 
by  dynamic  action,  which  has  also  occasioned  considerable  chemical 
changes.  These  rocks,  while  they  show  remains  ot  their  original  min- 
erals, have  become  decidedly  schistose  ; and  by  the  alteration  in  their 
composition,  they  have  developed  certain  other  points  of  similarity 
with  the  schists  at  g , into  which  they  appear  gradually  to  pass.  For 
this  reason  they  have  been  selected  to  represent  the  third  and  most 
altered  stage  of  the  gabbro  in  which  any  sure  signs  of  the  original 
character  of  the  rock  still  remain ; at  the  same  time  they  possess  even 
more  of  the  characters  belonging  to  the  schists,  and  thus  afford  just 
the  evidence  desired  that  the  latter  are  the  extremely  modified  form  of 
the  massive  rock. 

No.  11166  is  only  indistinctly  schistose,  showing  a soft  grayish  green 
matrix  in  which  are  imbedded  altered  grains  of  a reddish  feldspar. 
Under  the  microscope  the  original  coarsely  granular  structure  of  the 
rock  may  still  be  made  out.  Large  but  much  broken  areas  of  feldspar 
may  be  clearly  seen  where  but  very  little  of  the  unaltered  substance 
remains.  For  the  most  part  this  has  been  changed  to  an  aggregate  of 
calcite  and  minute,  brightly  polarizing  needles  or  plates  of  a colorless 
micaceous  mineral  (probably  sericite)  aloug  with  occasional  areas  of 
secondary  quartz.  What  was  once  the  pyroxene  or  hornblende  is  now 
a colorless  or  extremely  pale  green,  scaly  mineral  which  an  examination 
shows  to  be  chlorite.  Between  crossed  nicols  it  is  isotropic  or  very 
feebly  polarizing.  It  was  separated  by  the  Thoulet  solution  from  the 
slightly  heavier  feldspar  and  as  a powder  appears  pale  green.  In  a 
closed  tube  it  gives  off  water  abundantly  and  becomes  dark.  With  hot 
sulphuric  acid  it  decomposes  and  gelatinizes  immediately ; with  hydro- 
chloric acid  it  decomposes  slowly,  givinga  somewhat  yellowish  solution, 
from  which  ammonium-hydroxide  precipitates  alumina  abundantly. 
There  can  therefore  be  no  doubt  that  this  mineral  is  a chlorite  very  poor 
in  iron,  like  the  nearly  colorless  pyroxene  from  which  it  is  derived. 
Areas  of  leucoxene  are  also  common  through  this  rock. 

No.  11165,  taken  from  a place  only  a foot  or  two  below  the  last  and 
undoubtedly  continuous  with  it,  is  decidedly  more  schistose.  Under 
the  microscope  the  minerals  are  essentially  the  same  as  in  the  last 
specimen,  but  the  mechanical  effects  here  exhibited  are  much  more 
intense.  The  feldspar  and  the  diallage  are  still  recognizable,  but  the 
colorless  chlorite  is  much  more  abundant  than  in  any  specimen  before 
described.  The  feldspar  areas  have  a brownish  color,  even  in  the  thin 
section  and  they  are  pulled  and  torn  asunder  in  a remarkable  man- 
ner. Individuals  are  often  pulled  out  into  more  than  twice  their  orig- 
inal length,  the  separation  taking  place  along  a series  of  interlacing 
cracks  which  run  approximately  perpendicular  to  the  schistose  structure 


74 


GREENSTONE  SCHIST  AREAS  OF  MICHIGAN. 


[BULL.  62. 


of  the  rock.  The  spaces  between  the  separated  fragments  are  filled 
with  the  chloritic  mineral.  This  rock  shows  every  indication  of  having 
been  enormously  stretched  and  this  process,  along  with  attendant 
chemical  changes,  has  induced  its  schistose  structure.  Although  it 
shows  under  the  microscope  traces  of  the  original  gabbro  structure  and 
of  the  original  gabbro  minerals,  no  one  would  hesitate  from  a micro- 
scopical examination  to  class  it  with  the  schists. 

The  schists  above  mentioned  as  occurring  between  the  two  masses 
of  typical  gabbro,  li  and /,  at  the  Sturgeon  Falls,  possess  an  important 
relationship  to  these  rocks.  Taken  by  themselves,  they  offer  as  rep- 
resentative examples  of  fissile,  silky,  hydro- mica  or  sericite  schists  as 
could  anywhere  be  found,  and  yet  this  narrow  band  presents  such  a 
complete  series  of  transition  forms  that  their  origin  as  derivatives  of 
the  massive  rock  cannot  be  doubted.  In  fact,  two  such  series  were 
traced  out  in  detail.  One  of  these  was  collected  on  the  lower  side  of 
h and  represents  the  passage  of  the  least  altered  and  most  massive 
gabbro  into  the  typical  schist,  and  the  other  was  obtained  near  the 
center  of  the  schist  band  where  a narrow  strip  of  the  rock  has  hap- 
pily been  preserved  from  the  extremest  alteration  and  plainly 
shows  its  identity  with  the  gabbro  proper.  This  narrow  layer,  rep- 
resented on  the  map  at  g , is  of  great  value  in  conclusively  proving  the 
origin  of  the  schists  in  the  midst  of  which  it  lies  and  into  which  it 
passes  on  both  sides. 

No.  11160,  from  this  locality  ( g ),  was  classified  in  the  field-notes  with 
the  schists,  and  regarded  as  only  a harder  and  more  slaty  form  of  these. 
Indeed,  this  rock  is  very  schistose,  cleaving  readily  in  a direction  par- 
allel to  the  foliation  of  the  more  fissile  schists.  Under  the  microscope, 
however,  an  original  gabbro  structure  is  still  distinctly  seen.  Triclinic 
feldspar,  in  broken  and  bent  crystals,  is  plainly  visible,  while  the  other 
constituents  have  passed  into  colorless  chlorite,  quartz  and  calcite. 
The  feldspar  itself  is  mostly  altered  into  the  same  compounds,  though 
its  form  and  occasionally  its  twinning  striae  are  still  preserved. 

No.  11161  is  a hard,  greenish  slate,  occurring  beside  the  last  described 
rock.  Under  the  microscope,  in  ordinary  light,  crystal  forms  are  seen 
outlined  in  a dark  color,  the  matrix  being  colorless.  In  polarized  light, 
however,  these  are  no  longer  visible,  and  there  is  only  a fine  grained 
and  schistose  aggregate  of  colorless  chlorite,  quartz  and  calcite. 

Nos.  11159  and  11158,  collected  just  below  the  last,  are  typical  schists 
of  a light  gray  color  and  somewhat  greasy  feel.  They  contain  just  the 
same  minerals  as  the  rocks  last  described,  but  here  every  trace  of  orig- 
inal structure  has  disappeared.  There  is  no  indication  of  the  form  of 
any  earlier  constituents,  but  those  now  present  are  arranged  in  a finely 
parallel  mosaic  of  somewhat  varying  grain.  Calcite  is  much  more 
abundant  than  in  the  previous  instances.  Indeed,  in  No.  11158  this 
mineral  makes  up  a large  share  of  the  rock. 

The  other  series  of  transition  forms  between  the  gabbro  and  the 


WILLIAMS.  J 


SCHISTS  DERIVED  FROM  THE  GABBRO. 


75 


schists  occurs  on  the  lower  side  of  the  gabbro  mass  h.  This  series  em- 
braces the  specimens  of  the  first,  second,  and  third  stages  of  the  gabbro 
already  described  from  this  exposure,  and  terminates  with  two  speci- 
mens of  schist,  Nos.  11163  and  11164.  Any  sharp  line  of  demarkation 
between  the  typical  and  massive  saussnrite-gabbroat  /*,  and  the  fissile, 
silvery  schists,  apparently  so  different,  lying  below  it,  was  sought  long 
and  carefully,  but  in  vain.  In  fact  no  such  line  exists,  and  if  one  were 
to  be  drawn  it  must  be  drawn  arbitrarily.  The  rocks  already  described 
from  this  locality  as  specimens  of  the  gabbro  in  the  third  stage  show 
this.  No.  11165  is  entered  in  the  field-notes  as  belonging  to  the 
schists,  but  microscopical  examination  shows  it  to  be  even  more  closely 
allied  than  the  almost  massive  No.  11166,  to  the  gabbro.  Traces  of  the 
original  components  and  structure  are  by  no  means  rarest  in  those 
rocks  which  appear  macroscopically  to  have  suffered  the  most  profound 
alteration. 

Nos.  11164  and  11163  are  light  gray,  silvery  schists,  with  a somewhat 
greasy  feel;  such  in  fact  as  might  ordinarily  be  classed  as  sericite  or 
hydro-mica,  schists.  Their  lamination,  however,  is  not  in  the  least  regu- 
lar, but  undularory,  aud  there  is  a tendency  to  cleavage  not  so  much 
along  a single  plane  as  in  almost  any  plane  parallel  to  a line.  In  other 
words,  these  rocks  have  a well  marked  dip,  but  hardly  any  determina- 
ble strike.  In  11164  especially,  there  is  noticeable  a jointing  trans- 
verse to  the  strike,  and  these  joint  planes  often  gap  open  into  wide,  len- 
ticular seams,  as  though  the  rock  had  been  stretched  in  the  direction 
of  its  strike. 

Under  the  microscope  these  rocks  are  seen  to  be  mostly  composed  of 
the  nearly  colorless  chlorite,  calcite,  and  a little  secondary  quartz. 
These  minerals  are  interlaced  in  narrow,  wavy  bands,  producing  what 
may  be  called  after  the  German  idiom,  a long  “ micro  flaser  v structure. 
But  even  here  every  trace  of  the  original  constituents  has  not  yet  dis- 
appeared. Occasional  battered  and  broken  feldspar  remnants  are  en- 
countered, with  their  fragments  widely  separated,  and  for  the  most  part 
changed  to  sericite  or  calcite.  Around  these  curve  and  twist  the  silky 
chlorite  bands  developing  a sort  of  “Augen”  structure,  which  may  be 
best  seen  by  examining  a section  with  an  ordinary  pocket  lens.  The 
areas  of  leucoxene  also,  before  observed,  are  not  lacking  here,  but 
these  are  pulled  out  in  the  direction  of  the  schistose  structure,  un- 
til a single  one  may  be  followed  nearly  across  an  entire  section.  The 
bisilicates  have  evidently  all  passed  into  the  colorless  chlorite,  aud  this 
mineral  on  account  of  its  pliability  has  easily  accommodated  itself  to 
the  circumstances,  and  has  developed  the  pronounced  schistose  struct- 
ure which  is  now  the  most  important  feature  of  the  rock. 

These  rocks  are  schists,  indeed,  of  the  most  characteristic  type,  but 
in  the  light  of  their  field  relations  and  still  more  from  the  evidence 
which  a microscopical  study  of  the  whole  series  has  afforded,  it  is  evi- 
dent that  they  represent  the  most  altered  form  of  the  massive  gabbro, 
between  two  areas  of  which  they  are  included. 


76 


GREENSTONE  SCHIST  AREAS  OF  MICHIGAN. 


[BULL.  62. 


Chemical  analyses.—  In  order  to  ascertain  what  changes  have  taken 
place  in  the  chemical  composition  of  the  Sturgeon  Falls  gabbro  during 
the  process  of  its  alteration  into  the  schists,  the  following  analyses  of 
specimens  illustrating  three  successive  stages  of  the  alteration  were 
made  by  Mr.  E.  B.  Eiggs : 


I. 

II. 

III. 

Si02 

51.46 

38.05 

45.  70 

A1203  

14. 35 

24.  73 

16.  53 

Fe2o3 

3.  90 

5. 65 

4.  63 

FeO 

5.  28 

6. 08 

3.  89 

CaO 

9.08 

1.25 

4.  28 

MgO 

9.  54 

11.58 

9.  57 

XajO 

2. 92 

2.  54 

.55 

K20 

.24 

1.94 

3.82 

H20 

3.30 

7.53 

4.  70 

C02 

.20 

.93 

5.  95 

Total 

100. 27 

100.  28 

99.  62 

Rock  powder  dried  at  105°  C. 

I.  No.  11170,  freshest  gabbro  from  the  point  h. 

II.  No.  11166,  gabbro  in  third  stage  from  the  south  side  of  li. 

Iir.  No.  11164,  silvery  schist  from  between  g and  h. 

At  first  glance  these  analyses  seem  to  present  a curious  anomaly. 
The  intermediate  rock,  No.  11 166,  appears  to  differ  more  from  the  orig- 
inal type  than  the  most  altered  specimen,  No.  11164.  A closer  exam- 
ination, however,  shows  that  the  nature  of  the  chemical  processes  which 
have  gone  on  in  the  two  cases  is  essentially  different.  In  the  first  case, 
No.  11166,  this  has  been  chiefly  chloritization,  while  in  the  second  case, 
No.  11164,  the  chloritization  has  been  less,  but  sericitization  and  car- 
bonatization  have  also  been  extensive. 

The  abundance  of  the  colorless  chlorite,  above  described  as  present 
in  No.  11166,  here  manifests  itself  in  the  very  low  percentage  of  silica 
and  in  the  correspondingly  high  percentage  of  alumina,  together  with 
the  increase  of  both  magnesia  and  water.  The  iron  is  unusually  low 
in  this  chlorite  because  it  did  not  exist  in  the  mother  rock;  still  there 
has  been  a gain  rather  than  a loss  of  this  ingredient.  The  lime  has 
here  been  to  a great  extent  removed,  presumably  in  the  form  of  the 
soluble  bicarbonate,  while  the  slight  sericitization,  above  mentioned  in 
the  description  of  this  rock,  is  indicated  by  the  increase  of  the  potash. 

In  the  analysis  of  No.  11164,  the  less  extent  of  the  chloritization  is 
shown  by  the  less,  although  proportionate,  increase  of  alumina  and 
water  and  decrease  of  silica,  while  the  iron  and  magnesia  remain  about 
the  same  as  in  the  mother  rock.  Here  the  lime  has  been  partly, re- 
moved as  before  and  partly  retained  as  calcite,  visible  everywhere 
through  the  Tock  and  indicated  in  the  analysis  by  the  5.95  per  cent  of 
C(J2.  The  sericitization,  so  apparent  under  the  microscope,  is  here 
shown  by  the  great  increase  in  potash  and  the  exchange  of  the  soda 
for  potash. 


WILLIAMS.] 


LOWER  QUINNESEC  GREENSTONE. 


77 


LOWER  OR  LITTLE  QUINNESEC  FALLS. 

The  rock  exposure  of  Lower  Quinnesec  Falls  is  not  confined  to  the 
immediate  vicinity  of  the  falls  but  it  extends,  especially  on  the  left 
bank  of  the  river,  for  a considerable  distance  below.  This  portion 
forms  a high,  abrupt  and  homogeneous  ridge,  of  uniform  composition 
and  structure,  the  description  of  which  may  be  advantageously  sepa- 
rated from  that  of  the  rocks  occurring  immediately  at  the  falls. 

We  shall,  therefore,  consider  under  two  successive  heads: 

(Id  The  greenstones  of  the  so-called  “ Gabbro  Ridge”  of  Major  Brooks. 

(2)  The  greenstones  of  the  Lower  Quinnesec  Falls. 

Greenstones  of  the  so-called  “ Gabbro  Ridge”  of  Major  Broolcs. — For  a 
mile  below  Lower  Quinnesec  Falls,  the  north  bank  of  the  river  is  skirted 
by  an  almost  perpendicular  wall  of  massive  greenstone.  This  wall  is 
sometimes  over  a hundred  feet  in  height,  and  has  every  appearance  of 
being  a great  dike.  Although  for  the  most  part  it  is  quite  massive,  it 
presents  frequent  and  very  instructive  evidence  of  the  effect  of  great 
pressure  upon  it.  It  is  seamed  and  gashed,  broken  and  torn,  and  con- 
tains schistose  bands  of  varying  width.  Since  the  continuity  of  these 
bands  with  the  massive  rock  is  established,  their  study  is  calculated 
to  throw  light  on  the  subject  of  dynamical  metamorphism. 

Major  Brooks  designated  the  rock  which  composes  this  ridge  as  a 
“massive  gabbro,”  aud  correlated  it  with  the  above-described  saussu- 
rite-gabbro  of  Sturgeon  Falls.  My  studies  have,  however,  failed  to 
disclose  in  this  rock  any  trace  of  pyroxene.  In  addition  to  its  feld- 
spathic  constituent,  which  is  generally  altered  to  saussurite,  it  contains 
in  abundance  that  peculiar  pale  green  and  more  or  less  fibrous  variety 
of  hornblende  which  is  quite  universally  conceded  to  be  of  secondary  ori- 
gin. What  the  primary  form  of  all  this  green  hornblende  was,  it  is  now 
impossible  to  ascertain  with  certainty.  It  is  of  a kind  well  known  to 
originate  from  the  alteration  of  pyroxene.  The  rock  as  a whole  also 
bears  decidedly  the  character  of  a diabase  or  pyroxene  rock;  and  yet, 
not  a trace  of  pyroxene  has  been  discovered  in  any  of  the  Menominee 
River  greenstones,  if  we  except  the  light  colored  diallage  of  the  Stur- 
geon Falls  gabbro.  Whenever  the  pale  green  hornblende  can  be  traced 
back  to  an  original  form,  it  is  seen  to  be  derived  from  a compact 
brown  or  basaltic  hornblende.  This  fact  was  substantiated  not  merely 
for  the  rock  composing  the  ridge  here  under  discussion,  but  it  is  also 
true  foi  the  several  other  localities  examined  on  the  river. 

This  brown  hornblende  is  seen  first  to  turn  green  by  a reduction  of 
its  iron  to  the  ferrous  state,  or  to  become  bleached  by  loss  of  its  iron, 
and  finally  to  break  up  into  an  aggregate  of  fine  hornblende  needles 
exactly  similar  to  that  commonly  formed  by  the  alteration  of  pyroxene 
to  uralie. 

It  is,  of  course,  impossible  to  prove  that  some  of  the  secondary  fibrous 
hornblende  has  not  been  derived  from  pyroxene.  Indeed,  it  seems  very 
probable  that  both  augifce  and  compact,  brown  hornblende  may  have 


78 


GREENSTONE  SCHIST  AREAS  OF  MICHIGAN. 


[BIH.L.  62. 


existed  side  by  side  as  original  constituents  of  the  rock,  and  that  both 
finally  succumbed  to  the  same  process  of  alteration,  although  the  horn- 
blende resisted  this  much  longer  than  the  augite.  Such,  in  point  of 
fact,  has  elsewhere  been  observed  to  be  the  case  where  both  minerals 
have  undergone  uralitization  in  the  same  rock;1  and  this  would  account 
for  the  frequent  survival  of  brown  hornblende  cores  where  every  trace 
of  pyroxene  had  disappeared. 

If  this  is  not  the  true  explanation  of  the  genesis  of  these  rocks,  there 
are  but  two  other  hypotheses  possible — either  that  the  original  rock 
contained  no  pyroxene,  but  was  a diorite,  composed  of  plagioclase  and 
brown  hornblende ; or,  that  the  pyroxene  has  passed  into  uralite  through 
an  intermediate  compact,  brown  hornblende.  Opposed  to  the  first  of 
these  suppositions  is  the  structure  of  the  rock,  which  is  diabasic  rather 
than  dioritic.  On  the  other  hand,  considerable  evidence  afforded  by 
various  of  the  Menominee  rocks,  as  well  as  observations  made  elsewhere 
by  the  writer2  and  by  Lossen,3  indicate  that  the  latter  hypothesis  may 
possibly  be  true.  Inasmuch,  however,  as  the  rocks  here  under  discuss- 
ion afford  no  trace  of  pyroxene,  it  hardly  seems  justifiable  to  call  them 
anything  but  diorite.  We  shall  encounter  still  more  distinct  examples 
of  this  type  farther  up  the  river. 

All  the  specimens  collected  from  this  greenstone  ridge  show  an 
advanced  stage  of  alteration.  Some  obtained  from  the  western  ex- 
tremity of  the  ridge,  near  the  Michigan  bank  of  Lower  Quinnesec 
Falls,  have  a coarsely  porphyritic  structure,  and  are  among  the  freshest 
specimens  that  were  procured.  This  variety  of  the  rock  is  represented 
by  Nos.  11034,  11035,  and  11098.  Of  these  the  last  is  perhaps  the  most 
typical.  To  the  unaided  eye  it  shows  a light  greenish  gray  matrix, 
thickly  studded  with  irregularly  shaped  crystals  of  opaque  white  feld- 
spar (saussurite)  from  one-halt  centimeter  to  two  centimeters  in  diame- 
ter. A closer  examination  reveals  many  brightly  reflecting  cleavage 
surfaces  of  another  and  darker  mineral.  These  are  of  about  the  same 
size  as  the  feldspar  crystals,  but  their  continuity  is  interrupted  by  small 
opaque  spots,  which  produce  the  mottled  structure  recently  termed  by 
the  writer  pcecilitic .4  The  color  of  these  cleavage  surfaces,  which  with 
the  aid^of  the  microscope  are  found  to  belong  to  large  individuals  of  a 
somewhat  altered  hornblende,  is  so  nearly  like  that  of  the  ground  mass 
of  the  rock  that  unless  their  reflection  is  caught  in  just  the  right  light 
they  escape  detection. 

The  large  porphyritic  crystals  of  feldspar  are  almost  wholly  changed 
to  saussurite.  This  has  a dull  gray  color,  and  is  nearly  opaque  even  in 
the  thinnest  sections.  A high  magnifying  power  resolves  it  into  an  ag- 
gregateof  minute  zoisite  needles.  Curiously  enough,  these  feldspar  crys- 
tals show  a clear  zone  of  unaltered  substance  around  their  outer  edge. 

1 Bull.  U.  S.  Geol.  Survey,  No.  28,  p.  45. 

2Ara.  Jour.  Sci.,  3d  series,  vol.  28,  p.  262,  Oct.,  1884. 

3 Jahrbuch  preuss.  geol.  Landesanstalt  fur  1883,  p.  632,  Berlin,  1885. 

4 From  7roifciAo9,  mottled.  See  Am.  Jour.  Sci.,  3d  series  1886,  vol.  31,  p.  30. 


WILLIAMS.] 


ALTERATION  OF  THE  HORNBLENDE. 


79 


This  fresh  and  finely  striated  portion  presents  a striking  contrast  to  the 
dull  gray  saussurite,  and  it  is  difficult  to  imagine  how  it  has  so  com- 
pletely escaped  the  alteration  which  has  attacked  the  rest  of  the  crys- 
tal, unless  it  is  the  product  of  a more  recent  growth. 

With  the  exception  of  groups  of  ilmenite  grains,  which  are  beauti- 
fully fringed  with  a leucoxene  border,  the  remainder  of  this  rock  is  com- 
posed almost  wholly  of  hornblende.  In  its  freshest  state  this  mineral 
has  a compact  structure  and  coffee  brown  color,  with  the  usual  pleO- 
chroism  and  other  optical  properties  of  the  species.  Its  first  phase  of 
alteration  consists  in  turning  green,  and  this  is  followed  by  a gradual 
bleaching.  This  process  continues  until  the  mineral  has  become  quite 
colorless,  without,  however,  losing  its  compact  structure.  In  the  larger 
individuals  of  compact  hornblende,  whether  this  is  brown,  green,  or  color- 
less, occur  numerous  small  lath-shaped  feldspars,  which  produce  the 
mottled  or  “pcecilitic”  structure  above  alluded  to.  These  seem  to  be 
less  completely  changed  to  saussurite  than  the  larger  feldspar  crystals, 
but  they  often  contain  the  zoisite  crystals  in  a more  perfect  state  of 
development. 

It  has  already  been  mentioned  that 
these  hornblende  crystals  show  an 
advanced  stage  of  alteration.  The 
hornblende  itself  is  bleached  until  it 
is  nearly  colorless.  The  final  change 
seems  to  be  the  breaking  up  of  this 
bleached  hornblende  into  an  aggre- 
gate of  colorless  needles,  resembling 
tremolite.  In  other  cases,  however, 
it  is  changed  in  irregular  patches  to 
a colorless  chlorite  which  is  quite 
isotropic,  and  only  visible  between 
crossed  nicol  prisms.  The  peculiar 
manner  in  which  this  takes  place  de- 
serves particular  notice,  and  is  repre- 
sented in  Fig.  9.  The  hornblende 
substance  remains  in  interlacing  veins  between  the  chlorite  areas. 
It  is  brightly  polarizing  and  may  be  often  seen,  as  in  the  figure,  to 
be  continuous  with  an  unchanged  hornblende  individual.  This  peculiar 
mode  of  alteration  is  doubtless  also  conducive  of  the  “ pcecilitic”  effect 
above  mentioned.  The  clearness,  transparency,  refraction,  etc.,  of  both 
hornblende  and  chlorite  are  so  nearly  identical  that  this  structure  is 
wholly  invisible  in  ordinary  light,  and  the  effect  of  polarized  light  in 
transforming  the  apparently  homogeneous  and  colorless  mass  into  its 
two  strongly  contrasted  elements  is  very  striking. 

No.  11034  is  essentially  the  same  as  the  specimen  just  described, 
except  perhaps  that  it  is  more  altered,  and  hence  contains  less  of  the 
original  compact  brown  hornblende.  Most  of  the  hornblende,  indeed, 


80 


GREENSTONE  SCHIST  AREAS  OF  MICHIGAN. 


[BULL.  62. 


in  this  rock  is  colorless,  and  much  of  it  is  fibrous.  That  which  still 
retains  any  color  is  for  the  most  part  green. 

No.  11035  was  not  sectioned,  but  in  the  hand-specimen  it  exactly 
resembles  the  others. 

No.  11032,  collected  with  the  specimens  last  described,  is  a beautiful, 
fresh  looking  rock,  without  porphyri tic  structure,  but  with  its  hornblende 
in  long,  slender,  greenish-black  crystals.  Under  the  microscope  the 
feldspar  of  this  rock  is  seen  to  be  less  altered  than  in  those  above 
described.  Saussurite  is  abundantly  developed  in  it,  but  not  so  exten- 
sively as  in  the  porphyritic  crystals  of  the  other  specimens.  There  is, 
however,  here  no  brown  hornblende.  This  mineral  is  all  of  a pale  green 
color,  or  it  is  changed  to  chlorite,  which  sometimes  contains  sharp 
crystals  of  epidote.  Ilmenite  is  abundant  and  is  fringed  with  leu- 
coxene. 

The  above  described  specimens,  from  the  extreme  western  edge  of 
the  ridge  near  the  falls,  although  they  are  the  least  altered  form  of  the 
rock,  hardly  represent  its  most  typical  aspect,  as  the  ridge  is  followed 
along  the  river  bank,  westward  from  Sandy  Portage,  its  high  and  almost 
perpendicular  front  is  found  to  be  composed  of  a light  green  or  grayish- 
green,  fine  grained  or  aphanitic  rock.  This  is  compact  and  massive  in 
structure,  but  everywhere  profoundly  seamed  and  jointed.  It  is  cut  by 
cross-gashes  aud  parted  joints,  and  gives  every  indication  of  having 
been  pulled  or  crushed — at  all  events,  of  having  been  subjected  to 
enormous  mechanical  strains.  The  joints  and  seams  often  run  in  many 
different  directions,  producing  a regular  breccia  without  cement.  The 
rock  is  also  much  slickensided,  frequently  so  much  so  as  to  produce  a 
schistose  structure.  The  layers  thus  formed  sometimes  bend  around 
more  massive  cores,  which  seem  to  have  resisted  the  rubbing  action. 

The  formation  of  what  are  above  described  as  “cross-gashes”  is 
very  curious.  At  times  the  entire  face  of  the  rock  wall  is  scarred  with 
approximately  parallel  gaping  seams,  closely  resembling  the  rents  formed 
in  moderately  dry  clay  or  putty  when  this  is  stretched.  A single  open- 
ing does  not  extend  for  any  great  distance,  but  a great  number  of  them 
of  all  dimensions,  closely  crowded  together,  may  produce  an  irregular 
sort  of  foliation.  The  general  appearance  of  a rock  thus  gashed  is  rep- 
resented in  Fig.  10,  which  was  drawn  from  a hand-specimen.  This  of 
course  can  give  only  an  approximate  idea  of  the  appearance  of  this 
structure  in  a large  rock-mass.  These  gashes  seem  to  have  been  pro- 
duced by  a stretching  of  the  rock,  or,  what  amounts  to  the  same  thing, 
by  a bulging  perpendicular  to  the  action  of  some  great  pressure.  They 
resemble  the  “ Idaffende  Bisse described  by  Heim  in  the  Alps,  and  al- 
ready mentioned  in  Chapter  I ( p.  43).  The  edges  of  the  seams  are  ragged 
as  though  they  had  been  formed  by  a forcible  tearing  asunder  of  the 
rock  after  it  was  solid.  They  are  often  filled  with  subsequent  infiltra- 
tions of  secondary  minerals,  like  calcite  or  quartz,  but  more  frequently 
they  are  open. 


STRETCHED  GREENSTONE. 


81 


WILLIAMS.  J 

No.  11028  is  a fair  average  specimen  of  the  rock  composing  this  ridge. 
It  is  a grayish  green,  compact,  homogeneous  mass,  which  is  but  little 

jointed.  Under  the  microscope  it  is  seen  to  be  mainly  composed  of  a 

1 ‘ 


Fig.  10.— “ Cross-gashes”  in  a greenstone  from  Lower  Quinnesec  Falls. 

finely  fibrous,  pale  green  hornblende  of  secondary  origin,  of  saussurite, 
quartz,  and  ilmenite.  The  structure  of  the  rock  has  been  almost  en- 
tirely destroyed  in  the  course  of  the  mineralogical  changes  which  have 
taken  place  in  it.  As  the  new  minerals  have  formed  they  have  wan- 
dered from  the  position  occupied  by  the  older  ones  and  have  thus  pro- 
duced a fine  grained  and  confused  aggregate  in  which  remains  of  larger 
rectangular  feldspars  or  hornblende  crystals  are  only  rarely  discernible. 
The  ilmenite  is  scattered  about  in  minute  dots,  each  surrounded  by  its 
own  leucoxene  border.  The  quartz  is  in  irregular  patches  and  bears 
every  evidence  of  being  secondary  in  its  origin. 

No.  11033,  from  near  the  western  end  of  the  ridge,  is  almost  identical 
with  the  specimen  last  described,  but  contains  more  quartz,  and  the 
remains  of  the  feldspar  imbedded  in  a dark  gray,  opaque  matrix. 

No.  11031  is  a specimen  collected  from  very  near  the  spot  where  No. 
11028  was  obtained,  and  the  two,  when  taken  in  connection,  show  in  a 
very  clear  and  beautiful  manner  the  effect  of  mechanical  action  in  modi- 
fying both  the  macro-structure  and  the  micro-structure  of  a solid  rock. 

Bull.  02 0 


82  GREENSTONE  SCHIST  AREAS  OF  MICHIGAN.  [bull.  62. 

In  spite  of  great  present  differences,  there  can  be  no  doubt  that  the 
two  specimens  were  once  portions  of  a continuous  mass.  They  were 
taken  side  by  side  from  a single  ledge  which  showed  nothing  like  a line 
of  contact  between  two  different  rocks.  One  is  a typical  massive  green- 
stone, with  hardly  a joint-plane  visible  in  it;  the  other,  while  agreeing 
closely  with  the  first  in  color  and  texture,  is  deeply  cracked,  gashed 
and  seamed,  and  possesses  a pronounced  schistose  structure.  The  orig- 
inal form  of  both  specimens  was  doubtless  an  igneous  rock  of  the  dia- 
base type,  which  has  been  subjected  in  one  case  (Ho.  11028)  to  chemical 
(metasomatic)  and  in  the  other  (Ho.  11031)  to  dynamic  metamorphism. 

Rocks  may  be  altered  by  simple  pressure,  but  the  accumulated  strains 
which  are  generated  within  them  are  relieved  and  adjusted  by  over- 
coming the  force  of  cohesion  along  certain  planes.  Here  there  will  be 
a shearing  motion  of  greater  or  less  extent,  and  a consequent  crushing 
of  the  rock.  The  rent  is  soon  healed  by  the  crystallization  of  new  com- 
pounds which  cement  the  crushed  fragments,  and  in  this  way  a schistose 
band,  of  width  varying  with  the  intensity  of  the  force,  may  be  devel- 
oped in  the  midst  of  an  otherwise  solid  and  massive  rock ; or  a number 
of  such  bands  may  be  formed  parallel  to  one  another,  and  together  im- 
parting to  the  rock  the  appearance  of  a foliated  or  even  a banded 
schist. 

Conclusive  proof  of  this  process  might  be  difficult  to  discover  without 
the  aid  of  the  microscope,  but  this  instrument  is  happily  able  to  afford 
sufficient  evidence  to  overcome  all  doubt.  We  shall  have  many  instances 
of  such  action  to  describe  in  the  sequel,  each  of  which  will  exemplify 
some  particular  phase  of  the  process. 

The  two  rocks  here  under  discussion,  however,  illustrate  this  general 
principle  in  an  admirable  manner.  Plate  IX  represents  the  appearance 
of  each  of  them  in  a thin  section  as  seen  under  the  microscope.  The 
structure  of  the  first,  Ho.  11028,  is,  as  above  described,  a granular  aggre- 
gate of  fibrous  hornblende,  chlorite  saussuritized  feldspar,  quartz,  and 
ilmenite,  produced  by  chemical  action  alone  in  recrystallizing  the  ele- 
ments of  the  original  constituents  in  new  compounds  more  in  accord- 
ance with  the  altered  physical  conditions  to  which  the  rock  was  sub- 
jected. The  component  minerals  of  the  second  rock  (Ho.  11031)  are 
not  so  different  from  the  last,  but  the  story  of  its  origin  is  told  in  its 
structure.  The  primary  constituents  seem  to  have  been  literally  pul- 
verized by  crushing.  The  feldspar  crystals  have  been  pulled  apart, 
the  fragments  being  separated  a considerable  distance  (always,  how- 
ever, in  the  same  direction),  but  it  is  still  possible  to  recognize  frag- 
ments which  once  belonged  together.  The  substance  of  this  feldspar 
is  remarkably  fresh,  another  instance  of  the  chemical  action  which  takes 
place  in  this  mineral  being  inversely  proportional  to  the  mechanical 
action  which  has  affected  it.  The  separation  of  the  feldspar  fragments 
is  due  to  a stretching  action  and  the  spaces  between  them  are  filled 
with  a pale  green  and  almost  isotropic  chlorite.  This  mineral  has 


williams.]  PROCESS  OF  ALTERATION  IN  THE  GREENSTONES. 


83 


evidently  been  developed  at  the  expense  of  the  hornblende,  which  is 
here  only  rarely  to  be  found,  and  then  always  in  bauds  where  the  me- 
chanical deformation  has  been  less  intense.  Where  it  is  found,  how- 
ever, this  hornblende  is  identical  with  that  occurring  in  No.  11028.  The 
ilmenite  and  leucoxene  are  seen  as  before,  but  the  former  is  far  less 
abundant  while  the  latter  is  proportionately  more  abundant.  When 
the  ilmenite  has  completely  disappeared,  the  leucoxene  forms  bands  and 
stringers,  thus  aiding  in  the  production  of  a schistose  structure. 

This  development  of  chlorite  out  of  the  hornblende  substance  seems 
to  be  a very  important  feature  in  the  stretched  basic  eruptive  rocks 
and  many  other  instructive  examples  of  it  will  be  given  beyond.  It 
has  a definite  bearing  upon  the  origin  of  the  fine  grained  chlorite  schists 
which  accompany  and  are  interstratified  with  so  many  of  them. 

Nos.  11041  and  11042  form  an  instructive  pair  of  specimens,  collected 
near'  the  river  bank  toward  the  western  end  of  the  ridge.  At  this 
particular  locality  there  is  a well  marked  band  of  green  schist  travers- 
ing the  here  generally  massive  greenstone  in  a direction  8.  70°  E.  The 
schistose  structure  is  irregular  and  undulatory,  and  on  either  side  there 
is  a gradual  passage  from  the  schist  into  the  massive  rock.  No.  11042 
is  from  the  surrounding  mass  immediately  at  the  edge  of  the  schist 
band.  In  a hand- specimen  it  appears  to  be  considerably  altered,  of  a 
gray  color,  and  without  any  cleavage.  Under  the  microscope  the  orig- 
inal structure  i&  easily  recognizable.  The  rock  is  largely  composed  of 
stout  rectangular  feldspars,  with  a somewhat  rounded  outline,  and  in- 
ternally changed  to  saussurite,  though  their  periphery  is  mostly  clear. 
Between  these  are  the  remains  of  former  hornblende  (possibly  pyroxene) 
individuals  now  represented  only  by  amphibole  fibers  and  chlorite. 
Beautiful  skeleton  forms  of  leucoxene,  composed  of  three  sets  of  par- 
allel bands,  reproducing  the  rhombohedral  parting  of  the  original  ilrneu- 
ite,  are  abundant. 

No.  11041  is  the  same  rock  as  the  last  in  a much  more  altered  form. 
The  feldspar  is  mostly  changed  to  calcite,  and  the  hornblende  to  chlo- 
rite. The  structure  has  wholly  disappeared  and  there  is  a very  fine  mo- 
saic of  quartz  and  secondary  albite  substance.  Still,  the  same  skeleton 
forms  of  leucoxene  remain  and  there  is  no  doubt  that  the  two  speci- 
mens represent  the  same  rock  in  different  stages  of  alteration,  the 
more  changed  form  having  become  decidedly  schistose. 

Farther  west,  in  the  immediate  vicinity  of  Lower  Quinnesec  Falls,  the 
abrupt  face  of  the  diorite  ridge  proper  retires  a short  distance  from  the 
river  bank.  Along  the  shore  the  massive  greenstones  give  place  to  slaty 
rocks,  which  cleave  into  rhomboidal  prisms.  They  have  no  proper  strike, 
but  seem  to  break  with  equal  readiness  in  all  planes  parallel  to  a line; 
and  this  line  is  here  nearly  perpendicular 4o  the  surface.  No.  11043  is 
one  of  these  rocks  of  a greenish  color.  Under  the  microscope  it  is  seen 
to  have  been  so  profoundly  altered  that  it  is  now  impossible  to  assert 
from  internal  evidence  what  its  original  character  was.  Still,  its  geo- 


84 


GREENSTONE  SCHIST  AREAS  OF  MICHIGAN. 


[BULL.  62. 


logical  position  indicates  that  it  was  once  a part  of  thegabbro  or  diorite 
ridge,  and  there  is  nothing  in  its  present  structure  that  directly  contra- 
dicts this  supposition.  The  rock  has  a pronounced,  although  irregular 
and  undulatory,  schistose  structure.  It  consists  largely  of  a fine  grained 
matrix,  composed  of  chlorite  scales,  arranged  parallel  to  the  direction 
of  schistosity.  With  this  mineral  are  associated  quartz,  feldspar,  opaque 
black  grains,  probably  magnetite,  and  occasionally  sharply  defined  crys- 
tals of  muscovite.  Imbedded  in  this  groundmass  are  larger  feldspars, 
sometimes  in  well  developed  crystals,  sometimes  in  fragments.  The 
substance  of  these  is  but  very Tittle  altered,  and  yet  their  outline  is 
made  indistinct  by. the  penetration  into  them  of  the  chlorite  scales. 
They  often  appear  to  have  been  much  squeezed  and  broken,  the  frag- 
ments being  more  or  less  separated.  Grains  of  quartz  are  occasionally 
seen,  which  have  also  been  fractured  by  pressure.  Calcite,  due  to 
alteration,  is  also  sparingly  present. 

Similar  rocks,  more  or  less  schistose  and  varying  from  a dark  green 
to  a light  gray,  occur  from  this  point  along  the  river  bank  all  the  way 
to  the  falls. 

No.  1104G  is  from  the  light  silvery-gray,  greasy-feeling  baud,  which 
projects  into  the  basin  at  the  foot  of  the  falls.  This  is  a typical  sericite 
schist.  Under  the  microscope  it  is  seen  to  have  a finely  schistose  struct- 
ure, produced  by  the  parallel  arrangement  (often  in  bands)  of  quartz 
grains,  sericite  scales,  and  chlorite,  which  is  nearly  colorless.  Along 
with  this  is  a large  amount  of  calcite,  also  distributed  in  bands.  There 
is  no  feldspar  visible.  The  most  interesting  constituent  is  rutile.  This 
mineral  is  sparingly  distributed  through  the  whole  rock  in  very  minute 
and  sharply  defined  crystals.  These  have  a pale  yellow  color,  a high 
index  of  refraction,  and  the  usual  twinned  forms.  In  certain  portions 
of  the  section  there  are  dull  gray,  opaque  spots,  which  are  yellow  in 
reflected  light.  These  are  not  continuous,  but  are  more  or  less  broken 
up  and  pulled  out  in  the  direction  of  the  schistose  structure.  They 
contain  occasional  dark  red  and  irregularly  shaped  graius  of  rutile,  but 
for  the  most  part  they  are  composed  of  innumerable  small  rutile  needles 
(quite  like  the  u Thonschiefernadeln v of  the  Germans)  so  closely  crowded 
together  as  to  form  an  opaque  mass,  only  resolvable  with  a high  power 
of  the  microscope.  From  these  dense  masses  the  other  little  needles 
in  the  other  parts  of  the  rock  seem  to  have  wandered. 

This  rock  is  almost  identical  with  certain  light  colored,  very  fissile 
schists  occurring  on  the  opposite  side  of  the  river  (cf.  No.  11011,  de- 
scribed beyond),  and  the  strike  of  these  two  exposures  seems  to  identify 
them  as  belonging  to  a single  band. 

Greenstones  of  the  Lower  QiUnnesec  Falls. — Passing  now  to  the  rocks 
exposed  along  the  northern  or  northwestern  shore  of  the  basin  below 
Lower  Quinnesec  Falls,  we  find  alternating  bands  of  lighter  and  darker 
colored  greenstones,  each  accompanied  by  schistose  layers,  which  pre- 
sent instructive  examples  of  dynamic  metamorphism. 


85 


williams.]  SCHISTOSE  BANDS  IN  THE  GREENSTONES. 

The  accompanying  map  (PL  IV)  represents  an  enlarged  portion  of 
Major  Brooks’s  map  of  Lower  Quinnesec  Falls.  Commencing  at  the 
western  corner  of  the  basin  there  are,  along  its  northern  shore,  three 
bands  of  dark  and  two  of  light  colored  rocks.  The  two  kinds  of  struct- 
ure, massive  and  schistose,  are  so  intimately  connected  in  both  of  them 
that  it  is  impossible  to  escape  the  conviction  that  the  latter  has  been 
secondarily  developed. 

If  we  begin  at  the  extreme  western  end  of  this  exposure,  at  the  corner 
of  the  basin  where  a sharp  bend  in  the  river’s  course  has  produced  a 
low,  sandy  beach,  we  discover  that  the  rocks  are  of  a dark  green  color. 
The  first  specimen  taken  from  this  band  (No.  11001)  is  massive  and 
jointed.  No  feldspar  is  visible,  except  in  large  porphyritic  crystals, 
which  are  not  common.  Even  in  this  massive  rock  occasional  narrow 
bands,  having  a wavy  foliation,  may  be  seen.  These  resemble  slicken- 
sides,  and  represent  planes  of  slipping  or  sliding  in  the  massive  rock 
(No.  11002).  Tracing  these  rocks  a short  distance  to  the  east,  the  wavy 
schistose  bands  become  more  and  more  numerous,  until  the  whole  mass 
becomes  decidedly  slaty,  and  has  a greasy  feel.  This  foliated  rock 
strikes  slightly  south  of  east  and  dips  steeply  toward  the  north.  The 
laminae  are  frequently  separated  and  bulged  into  lenses,  which  are 
either  filled  with  quartz  or  are  still  open  and  then  coated  with  drusy 
quartz  (No.  11003).  These  slaty  rocks  have  a dark  gray  color,  and,  in 
some  respects,  resemble  hydro-mica  schists,  but  yet  it  is  impossible  to 
separate  them  in  the  field  from  the  dark  green  massive  rocks  above 
described,  as  each  passes  by  insensible  gradations  into  the  other. 

Under  the  microscope,  No.  11001  appears  as  a medium  grained  aggre- 
gate of  feldspar  and  pale,  fibrous  hornblende  with  some  ilmenite  and 
leucoxene.  The  structure  is  still  well  preserved.  The  feldspar  is  in 
stout,  columnar  crystals,  all  distinctly  striated  and  often  considerably 
changed  to  zoisite  or  epidote.  The  hornblende  is  in  irregular,  ragged 
masses  or  in  minute  needles.  The  pale,  fibrous  sort  is  plainly  seen  to 
have  been  derived  from  a compact,  darker  green  arid  pleochroic  variety ; 
but  farther  back  than  this  (i.  e.,  to  a possible  original  pyroxene)  it  can 
not  be  traced.  There  is  also  a little  pale  green  clilorite,  looking  much 
like  the  secondary  hornblende,  except  between  crossed  nicols,  where  it 
is  nearly  isotropic. 

No.  11002,  taken  from  one  of  the  narrow  schistose  bands,  has  plainly 
been  produced  by  a shearing  or  sliding  within  the  last  described  mas- 
sive rock,  and  presents  an  interesting  relationship  to  it  when  placed 
under  the  microscope.  The  two  are  plainly  identical  as  far  as  the  com- 
ponent minerals  are  concerned,  but  the  structure  of  the  latter  has  under- 
gone a great  change.  The  grain  at  first  glance  appears  to  be  finer,  but 
this  is  soon  seen  to  be  due  to  a crushing  of  the  original  minerals.  The 
feldspars  especially  are  very  much  broken  and  their  parts  more  or  less 
separated.  This  mechanical  action  has  been  attended  by  increased 
chemical  activity.  The  original  substance  of  the  crushed  feldspar  crys- 


86 


GREENSTONE  SCHIST  AREAS  OF  MICHIGAN. 


[bull.  62. 


tals  is  hardly  as  much  changed  as  in  the  preceding  instance,  but  there 
has  been  a considerable  recrystallization  of  new  feldspar  substance 
(probably  albite).  The  hornblende,  because  of  its  secondary  nature,  is 
more  like  that  in  the  massive  rock  (No.  11001),  but  even  this  is  some- 
times sundered  and  torn.  Chlorite  is  much  more  abundant,  especially  in 
the  interstices  between  the  fragments  of  the  broken  feldspar  crystals. 
It  is  sometimes  filled  with  very  delicate  and  minute,  though  extremely 
sharp,  epidote  crystals.  The  ilmenite  is  more  extensively  changed  to 
leucoxene  than  before,  and,  in  some  cases,  shows  a decided  pulling  out 
in  the  direction  of  the  schistose  structure.  On  the  whole,  many  of  those 
metasomatic  changes  which  the  greenstones  most  commonly  show  are 
here  seen  to  have  been  accelerated  and  intensified  by  the  mechanical 
force  which  has  crushed  the  rock  and  so  changed  its  structure.  Thus 
the  two  forces — dynamical  and  chemical — may  go  hand  in  hand  and 
together  produce  a rock  which  is  both  structurally  and  mineralogically 
very  different  from  that  out  of  which  it  has  been  derived. 

Passing  eastward  along  this  exposure,  we  next  come  to  a wide  band 
of  much  lighter  colored  rock,  which  extends  as  far  as  the  lower  side  of 
the  small  cove,  situated  on  the  right  bank  immediately  below  the  falls. 
This  band  exhibits,  in  a most  admirable  manner,  the  secondary  devel- 
opment of  schistose  layers  in  a massive  rock,  and  is  well  deserving  of 
careful  study.  The  most  typical  and  least  altered  form  occurs  just  at 
and  below  the  corner  of  the  small  cove.  This  is  a medium  grained, 
massive  aggregate  of  opaque  white  saussurite  and  light  green,  fibrous 
hornblende,  and  it  closely  resembles,  in  its  external  aspect,  the  barrier 
rock  at  both  Upper  Quinnesec  and  Sturgeon  Falls.  Nos.  11008  and 
11009  represent  this  occurrence,  but  even  the  most  massive  specimens 
which  could  be  obtained  are  seamed  with  cracks  approximately  parallel 
in  direction  and  coated  with  a lamellar,  soft  green  mineral  like  that  in 
the  adjoining  schists.  This  is  shown  by  examination  to  be  chlorite. 
On  both  sides  of  the  massive  portion  of  this  band  the  parallel  cracks 
become  more  and  more  abundant  (No.  11004  below,  and  No.  11010 
above),  and  on  the  lower  side  of  the  small  cove  the  rock  passes,  with- 
out any  break  in  its  continuity,  into  silky  schists  (No.  11011),  like  those 
above  described  from  the  opposite  side  of  the  river  (cf.  No.  11046,  p.  84). 

U nder  the  microscope,  the  least  altered  specimens  of  this  rock  (Nos. 
11008  and  11009)  are  found  to  bear  a close  resemblance  to  the  light 
colored  gabbro  of  Sturgeon  Falls  (see  p.  68),  except  that  in  the  present 
instance  no  trace  of  diallage  is  discernible.  The  structure  of  the  two 
rocks  is  the  same.  The  feldspar  is  here  also  replaced  by  the  same  gray, 
opaque  saussurite,  in  which,  with  a high  power,  zoisite  and  calcite  may 
be  easily  detected.  The  hornblende,  as  seen  in  a microscopic  section;  is 
practically  colorless.  Only  occasionally  are  traces  of  a greenish  tinge 
observable.  Between  crossed  nicols  this  mineral  generally  exhibits  a 
homogeneous  extinction,  so  that  it  can  not  be  regarded  as  truly  fibrous, 
and  yet  there  can  be  no  doubt  as  to  its  secondary  nature.  Its  edges  are 


u.  S.  GEOLOGICAL  SURVEY 


BULLETIN  NO.  62  PL. 


Dark  Diabase* 


Light  Schist^ 
Dark  Piabase^T^I 
Light  Gabbro-diqrite 
aftl  se.ricite  schists. 


JarkDiabasi 
aChlorite  ; 
Schists 


WISCONSIN 

T.  38JST.;R.20E. 


M!  I C H I G Ajn 
T.  3 9 _N".;R  -30  W. 


MAP 

of 

LOWER  QUINNESEC  FALLS 

Menominee  River 
(After  Brooks) 


SCALE 


Fee  i 


^Mile 


THt  UW»W 
Of  'Ht 

mwersw  of  fu»o» 


WILLIAMS.] 


EFFECT  OF  CRUSHING  ON  THE  FELDSPAR. 


87 


ragged  and  there  is  a decided  tendency  to  separation  into  fibersreven 
when  these  are  not  actually  present.  It  is  noteworthy  that  this  sec- 
ondary hornblende  can  only  be  traced  back  (and  that  in  rare  instances) 
into  a more  compact  greenish  or  brownish  variety  of  the  same  mineral. 
In  none  of  the  thin  sections  is  there  any  positive  evidence  that  dial- 
lage was  ever  present;  and  yet  the  close  similarity  of  this  rock  to  the 
Sturgeon  Falls  gabbro  naturally  suggests  it.  If  the  diallage  were 
originally  present  it  has  completely  changed  to  the  pale  hornblende, 
while  the  brown  hornblende  longer  resisted  the  bleaching  action,  and 
hence  sometimes  still  remains.  If  this  were  not  the  case,  we  are  com- 
pelled to  assume  one  of  the  two  other  alternatives  suggested  in  the 
case  of  the  porphyritic  diorite  from  the  other  side  of  the  river,  No. 
11098  (see  p.  78). 

The  pale  hornblende  is  often  partially  altered  to  colorless  chlorite, 
and  the  ilmenite  is  more  or  less  changed  to  leucoxene. 

Nos.  11004  and  11010,  taken  from  either  side  of  the  above  described 
band,  represent  somewhat  schistose  varieties  of  it  which  have  been 
produced  by  the  action  of  pressure , That  this  is  actually  the  case 
is  admirably  shown  by  a microscopic  examination.  The  hornblende 
of  the  original  rock  seems  to  have  passed  completely  into  a very  pale 
or  colorless  chlorite.  Saussurite,  on  the  Other  hand,  is  less  abundantly 
developed  than  in  the  more  massive  rock  above  described,  and  it  is  dis- 
posed in  narrow  veins  or  in  small,  irregular  spots.  The  ilmenite  has 
given  its  place  to  a dark  gray  substance  resembling  leucoxene.  This 
is  drawn  out  in  stringers  following  the  direction  of  the  schistosity, 
and  in  the  center  of  these  a yellow  grain  of  rutile  may  sometimes  be 
observed.  Galcite  is  also  present.  The  structure  of  the  rock  is 
completely  different  from  that  from  which  it  is  supposed  to  have  been 
derived.  It  is  now  composed  largely  of  a fine  grained  groundmass. 
This  is  made  up  of  a microgranitic  aggregate  of  minute  grains  of  an 
unstriated  substance  resembling  quartz,  but  which,  from  its  high  spe- 
cific gravity,  is  probably  a feldspar.  These  grains,  together  with 
chlorite  scales,  leucoxene,  some  calcite,  and  an  occasional  bit  of  epi- 
dote  or  sericite,  are  arranged  so  as  to  produce  an  indistinct  schistose 
structure,  the  bands  of  which  bend  and  wind  around  larger  porphyritic 
individuals  of  feldspar.  In  this  way  a lenticular  or  “ Flaser”  structure 
results,  which,  however,  is  hardly  discernible,  except  under  the  micro- 
scope. A very  particular  interest  attaches  to  the  porphyritic  feldspar 
crystals  of  these  rocks.  In  comparison  with  those  in  the  more  massive 
rock  (11008  and  11009),  they  are  but  slightly  altered  to  saussurite;  in- 
deed, for  the  most  part,  they  are  surprisingly  fresh  and  glassy.  Glis- 
tening cleavage  surfaces  may  be  readily  detected  with  the  unaided  eye, 
and  under  the  microscope  this  feldspar  appears  in  clear,  colorless  grains, 
almost  wholly  free  from  inclusions  of  any  kind.  Occasionally  these 
possess  a light  brownish  tinge,  due  to  some  evenly  distributed  pig- 
ment. Between  crossed  nicols  this  clear  feldspar  substance  presents 
sharp  twinning  lamella;  and  a comparatively  high  extinction  angle. 


88 


GREENSTONE  SCHIST  AREAS  OF  MICHIGAN. 


[BULL.  62. 


The  individual  crystals  are  invariably  broken  and  the  fragments  are 
more  or  less  separated.  The  intervening  spaces  are  filled  with  a micro- 
granitic  ground  in  ass,  as  shown  in  Plate  Till,  figs.  1 and  2,  of  other 
similar,  though  more  acid  rocks  from  Upper  Quinnesec  Falls  and  from 
the  vicinity  of  Marquette,  Michigan. 

The  clearness  and  freshness  of  this  feldspar  would  at  first  suggest  the 
probability  of  its  being  a secondary  crystallization,  as,  for  instance, 
albite  is  often  found  to  be.  This,  however,  is  shown  not  to  be  the  fact, 
first,  by  the  broken  state  of  all  the  crystals,  indicating  that  they  must 
have  been  in  existence  when  the  rock  was  pressed  and  crushed ; and, 
second,  by  their  physical  properties  which  show  that  the  feldspar  is 
labradorite.  Upon  isolation  this  feldspar  was  found  to  have  a specific 
gravity  of  2.69 ; and  in  cleavage  pieces  parallel  the  basal  plane,  it  gives 
an  extinction  augle  of  12°  to  20°  on  each  side  of  the  twinning- trace. 

The  survival  of  the  original  feldspar  in  an  almost  unaltered  state,  in 
a rock  so  profoundly  changed  by  mechanical  action,  naturally  occa- 
sioned some  surprise.  Examples  of  the  same  sort  have  already  been 
cited  (e.  g.  Nos.  11154  and  11165  from  Sturgeon  Falls,  and  No.  11032 
from  the  diorite  ridge  below  Lower  Quinnesec  Falls),  and  so  many  cases 
of  a like  character  were  encountered  from  other  localities  that  the  oc- 
currence of  the  freshest  feldspar  in  the  most  crushed  rock  must  be  re- 
garded as  the  rule. 

I know  of  no  way  of  interpreting  this  phenomenon,  substantiated  by 
so  many  instances,  except  by  supposing  that  the  pressure,  which  acts 
powerfully  in  stimulating  chemical  action  in  the  solid  rock,  is  relieved 
on  the  harder  grains  of  a crushed  band,  since  these  are  able  to  change 
their  position  by  slipping  among  the  softer  materials. 

The  nearly  vertical,  silvery  schists  (No.  11011)  which  occupy  the  west- 
ern corner  of  the  little  cove  just  below  the  Lower  Quinnesec  Falls,  rep- 
resent only  a more  highly  metamorphosed  state  of  the  rocks  above  de- 
srcibed.  They  are  extremely  soft,  fissile,  and  schistose  in  a hand-speci 
men.  Under  the  microscope  they  closely  resemble  the  groundmass  of 
the  last  described  rocks  (Nos.  11004  and  11010).  The  granular  aggre- 
gate is  so  disposed  as  to  produce  a decided  schistose  structure.  Both 
calcite  and  sericite  have  become  more  abundant,  while  the  porphyritic 
feldspar  crystals  have  completely  disappeared.  The  leucoxene  also  can 
nolougerbe  found,  but  the  long  lines  of  very  sharp  and  minute  rutile 
crystals,  which  are  not  present  in  any  of  the  more  massive  related  rocks, 
appear  to  have  taken  its  place. 

The  perfect  continuity  of  the  massive  rock  (Nos.  11008  and  11009) 
with  these  schists,  through  the  intermediate  member  (11010)  is  admira- 
bly shown  in  the  exposure  at  the  western  end  of  this  small  cove. 

The  following  chemical  analyses  of  these  three  specimens  have  been 
made  by  Mr.  K.  B.  Biggs. 


willtams]  ANALYSES  OF  LOWER  QUINNESEC  GREENSTONE.  89 

I.  No.  11008,  Gabbro-diorite  from  Lower  Quinnesoc  basin. 

II.  No.  11010,  Schistose  form  of  the  same  rock. 

III.  No.  11011,  Seriate  schist  adjacent  to  last. 


(I.) 

(II.) 

(III. ) 

Si02 

47.  96 

49. 19 

46.21 

ai2o3 

16.  85 

18.  71 

18.  38 

FfrjOj 

4.  33 

5.  03 

3.  30 

FeO 

4. 17 

4.04 

3.  90 

CaO 

13.  25 

5.  92 

6.  28 

MgO 

9. 15 

7.  98 

7.  03 

Xa20 

1.  25 

1. 44 

2. 14 

K20 

-.30 

.77 

.35 

H20 

2.  89 

5.  Q£ 

3.  82 

C02 

.08 

1.82 

8. 32 

Total 

100. 23 

99.  95 

99. 73 

Ti02  not  determined. 

The  close  agreement  between  these  analyses  is  striking.  The  low 
percentage  of  iron  sufficiently  accounts  for  their  uniformly  light  color. 
The  most  striking  difference  is  perhaps  the  loss  of  calcium  and  the 
lesser  loss  of  magnesium,  both  of  which  were  undoubtedly  carried  off 
in  the  form  of  soluble  carbonates  when  the  rock  was  crushed.  The 
water  is  contained  in  the  pale  chlorite,  which  first  increases  in  amount 
and  then  decreases,  as  its  components  are  transformed  into  carbonates. 
The  sodium  was  first  contained  in  the  feldspar  and  the  steady  increase 
in  its  relative  amount  is  probably  due  to  the  development  of  the  sericite- 
like  mica,  which  may  be  a paragonite. 

It  is  interesting  to  compare  the  first  of  these  analyses  with  that  of 
the  Sturgeon  Falls  gabbro  (I  on  p.  76),  the  close  resemblance  of  which 
to  the  rocks  here  under  consideration  has  already  been  alluded  to. 
The  only  noticeable  difference  is  a slightly  larger  proportion  of  silica 
and  a smaller  proportion  of  alumina  and  lime  in  the  Sturgeon  Falls 
rock. 

Passing  now  still  farther  to  the  eastward,  we  come  to  the  second  band 
of  dark-colored  greenstones  (see  map,  PI.  IY).  These  follow  directly 
after  the  narrow  exposure  of  the  above-mentioned  silvery  schists  in  the 
western  corner  of  the  little  cove  and  form  a great  part  of  its  northern 
shore.  They  resemble  the  rocks  occurring  in  the  band  first  described, 
and  present  both  massive  and  schistose  varieties,  which  grade  insensibly 
into  each  other  in  a manner  not  less  instructive  than  that  in  the  two 
bands  already  considered. 

Nos.  11012,  11013,  and  11021  (the  first  two  from  massive  portions  of 
this  band  along  the  shore  of  the  small  cove;  and  the  last  from  the  Wis- 
cousin  side  of  the  river  directly  opposite  the  falls)  are  essentially  identical 
in  appearance  and  composition.  In  the  hand-specimen  they  form  a 
compact,  aphanitic  mass,  of  a dark  green  color.  Under  the  microscope 
the  originally  diabasic  nature  of  the  rock  is  at  once  apparent,  although 


90 


GREENSTONE  SCHIST  AREAS  OF  MICHIGAN. 


[bull.  62. 


the  extensive  mineralogical  changes  which  have  gone  on  have  greatly 
obscured  its  former  structure.  The  components  now  present  are  al- 
most wholly  secondary.  These  are  hornblende,  chlorite  containing  epi- 
dote,  quartz,  and  leucoxene.  Ilmenite  and  occasional  traces  of  feldspar 
are  the  only  original  constituents  which  remain.  Still  the  disposition  of 
the  secondary  minerals  is  such  as  to  outline  a diabasic  or  ophitic  struct- 
ure often  with  great  distinctness.  The  feldspar  is  rarely  well  pre- 
served $ but  a narrow  zone  of  the  unaltered  substance  of  this  mineral 
often  outlines  a stoutly  lath-shaped  crystal,  even  when  its  interior  is 
wholly  changed  to  an  aggregate  of  quartz,  chlorite,  and  epidote.  The 
hornblende  has  a curious  appearance.  Its  crystals  are  brownish  and 
nonpleochroic  with  a somewhat  granulated  surface,  so  that  it  exter- 
nally resembles  diallage.  Its  cleavage  and  optical  properties  prove  it 
to  be  undoubtedly  hornblende,  although  this  superficial  likeness  to  di- 
allage  is  so  strong  as  to  almost  compel  the  conviction  that  it  has  origi- 
nated by  paramorphism  from  a pyroxene.  This  brown  hornblende  is 
seen  with  a high  power  to  be  gradually  changing  to  a green  variety,  in 
which  a pleochroism  for  the  first  time  becomes  apparent.  This  also 
frequently  passes  over  into  a fibrous  hornblende.  The  chlorite  epidote 
aggregate  in  these  rocks  is  very  finely  developed.  The  chlorite  is  of 
an  emerald  green  color  and  distinctly  pleochroic.  It  appears  between 
crossed  nicols  as  isotropic  or  polarizes  with  a maroon  tint.  The  epidote 
is  in  sharp,  light  yellow  crystals,  with  the  characteristic  shape  and  op- 
tical properties  of  this  species.  The  microscopic  appearance  of  this 
aggregate  is  represented  in  PI.  XI,  fig.  1,  drawn  from  a specimen 
collected  below  the  Upper  Quinuesec  Falls  (No.  11049).  The  literature 
relating  to  it  has  already  been  cited  (Chapter  I,  p.  57).  The  epidote 
crystals  have  been  described  from  the  Menominee  region  by  Wichmann1 
and  others  as  secondary  augite.  This  chlorite  epidote  aggregate  covers 
considerable  areas  and  occupies  the  place  of  both  the  feldspathic  and 
the  pyroxenic  constituents.  In  addition  to  the  minerals  already  named, 
ilmenite,  with  its  leucoxene  border,  pyrite  and  secondary  quartz  are 
quite  abundant  in  these  rocks. 

No.  11014,  taken  from  a narrow,  schistose  band  in  the  massive  green- 
stone (No.  11013),  shows  in  a remarkably  clear  manner  how  the  dy- 
namic metamorphism  of  this  rock  has  been  accomplished.  In  this  in- 
stance there  can  not  be  the  least  doubt  as  to  the  continuity  of  the  rock- 
mass.  The  hand-specimen  No.  11014  has  a decidedly  schistose  struct- 
ure, and  under  the  microscope  it  shows  the  effects  of  mechanical  crush- 
ing and  attendant  mineralogical  changes,  with  great  distinctness.  The 
whole  rock,  with  the  exception  of  certain  remains  of  the  larger  feldspar 
crystals,  has  been  reduced  to.  a fine  grained  mass,  showing  an  aggre- 
gate polarization.  Light  green  chlorite  has  been  largely  developed  and 
has  completely  replaced  all  the  bisilicate  elements.  The  parallel  ar- 
rangement of  the  scales  of  this  mineral  is  what  produces  the  schistose 


1 Geol.  Wisconsin,  vol.  3,  1876,  pp.  623,  624. 


Williams]  ANALYSES  OF  LOWER  QUINNESEC  GREENSTONE.  91 

structure,  and  it  surrounds  and  incloses  the  small  grains  in  the  man- 
ner which  has  already  been  explained  in  connection  with  No.  11031 
(p.  81 ) and  illustrated  in  PI.  IX,  fig.  2.  The  clear,  secondary  grains  form- 
ing this  mosaic  are  certainly,  to  some  extent  at  least,  quartz,  while  a 
portion  of  them  may  be  an  unstriated  feldspar.  Cal  cite  has  been 
largely  developed  in  the  schistose  rock,  and  the  leucoxene  is  replaced 
by  rutile,  either  in  stout,  yellow  grains,  or  in  minute,  sharp  crystals  ar- 
ranged in  long,  sinuous  lines. 

The  mechanical  action  which  produced  this  schistose  band  has  there- 
fore resulted  in  the  crushing  of  the  rock,  and  the  almost  total  disap- 
pearance of  all  of  the  original  components.  The  comparatively  slight 
change  in  the  chemical  composition  of  the  rock  as  a whole  may  be  seen 
from  the  two  following  analyses  of  Nos.  11021  and  11014,  made  by  Mr. 
B.  B.  Biggs. 

I.  No.  11021.  Dark  massive  greenstone,  Lower  Quinnesec  Falls. 

II.  No.  11014.  Dark  schistose  greenstone,  forming  a band  in  the  last. 


(I.) 

(II.) 

Si02 

43.  80 

44.  49 

A12Os 

16. 08 

16.  37 

Fe203 

9. 47 

5. 07 

FeO 

10.50 

5.  50 

CaO 

7.  81 

7.94 

MgO  

6.  54 

7.50 

Xa.20 

1.96 

2.  59 

K20 

0.  34 

0.  56 

H20 

3. 99 

4.99 

C02 

0.  08 

5.  38 

Total 

100.57 

100.  39 

Ti02  not  determined. 

Powder  dried  at  105°  C. 

The  changes  here  are  at  once  seen  to  be  due  (1)  to  the  total  removal 
of  the  iron  ores  (loss  of  iron) ; (2)  to  the  production  of  carbonates 
(gain  of  C(>2,  carbonatization) ; and  (3)  to  the  increase  in  the  amount  of 
chlorite,  (increase  of  H2G,  hydration). 

Toward  the  eastern  end  of  the  small  cove  the  dark-green  schistose 
rocks  appear  to  pass  by  insensible  gradations  into  exactly  similar  ones 
of  a lighter  color.  No.  11015,  one  of  these,  is  seen  under  the  micro- 
scope to  be  a very  schistose  aggregate  of  extremely  pale  chlorite  and 
quartz  grains.  There  is  a little  calcite  here  present  and  occasional 
scales  of  sericite.  The  rutile,  in  very  minute  and  sharp  crystals,  is  here 
crowded  into  long  bands  and  stringers  which  follow  the  schistosity  of 
the  rock  and  give  the  thin  section  a pronounced  “Flaser”  structure. 

No.  1 101 G,  from  the  extreme  eastern  corner  of  this  cove,  represents  a 
band  of  lightcolored  brownish  rocks  with  a perfectly  developed  schis- 
tose structure  and  a grain  somewhat  resembling  that  of  wood.  These 


92 


GREENSTONE  SCHIST  AREAS  OP  MICHIGAN. 


[bull.  62. 


stand  nearly  vertical,  though  some  dip  from  65°  to  70°  N.  20°  W. 
Their  strike  is  turned  from  that  of  the  other  rocks  here  (S.  70°  E)  some 
30°  to  40°,  so  that  they  now  strike  N.  70°  E.  Under  the  microscope 
this  rock  is  seen  to  have  essentially  the  same  structure  and  composition 
as  the  last.  The  main  difference  between  them  is  that  the  present  spec- 
imen has  a brown  chlorite  instead  of  a green  one.  This  it  is  that  im- 
parts the  peculiar  color  to  the  rock  in  the  hand-specimen.  There  is 
also  more  calcite  in  this  rock  than  in  the  other.  It  would  seem,  along 
with  No.  11011  above  described,  to  represent  the  most  profoundly  met- 
amorphosed phases  of  the  massive  rocks  at  Lower  Quinnesec  Falls. 

The  original  constituents  have  undergone  an  alteration  to  chlorite, 
quartz,  carbonates,  and  rutile.  The  iron  has  largely  disappeared,  and 
the  crystallization  of  the  new  components  under  lateral  pressure  has 
produced  a very  pronounced  schistose  structure. 

No.  11023,  from  the  upper  end  of  the  breakwater,  above  the  falls 
(Wisconsin  side),  is  very  closely  allied  to  the  two  specimens  last  de- 
scribed. It  is  a grayish  schist,  with  the  prevailing  strike,  but  every- 
where seamed  with  transverse  cross-gashes,  which  are,  for  the  most  part, 
filled  with  infiltrated  quartz.  There  seems  to  be  little  doubt  from  a 
field  examination,  that  this  rock  is  continuous  with  the  massive  diabase 
(No.  11021)  in  the  same  way  that  the  last  mentioned  specimens  are  con- 
tinuous with  Nos.  11012  and  1 1013.  The  massive  green  rock  (No.  11021) 
is  exposed  a very  short  distance  to  the  west  of  it,  where  it  also  is  filled 
with  seams  and  cross-gashes,  which  appear  to  have  been  squeezed  open 
by  lateral  pressure.  From  this  point  the  transition  to  the  gray  schis- 
tose rock  is  a very  gradual  one.  The  latter  rock  has  no  regular  bedding 
but  only  a cleavage  in  one  direction.  This  causes  it  to  break  out  in  angu- 
lar prisms.  The  rock  is  everywhere  fissured,  slickensided,  and  filled 
with  infiltration  quartz,  as  evidence  of  the  enormous  pressure  to  which 
it  has  been  subjected.  Under  the  microscope  it  is  much  like  No.  11016. 
There  is  the  same  quartz  mosaic,  pale  chlorite  and  strings  of  rutile 
needles,  arranged  so  as  to  produce  a decided  schistose  structure.  There 
is,  however,  in  this  rock  considerably  more  calcite  and  an  additional 
feature  in  the  way  of  remains  of  former  feldspar  crystals.  These  are 
considerably  altered,  and  appear  to  be  changing  to  a mass  quite  like  that  .* 
which  composes  the  rest  of  the  rock.  In  fact,  this  has  gone  so  far  that 
it  is  almost  impossible  to  distinguish  these  feldspars  in  ordinary  light, 
although  their  outline  and  nature  become  very  apparent  between  crossed  j 
nicols.  They  are  arranged  without  reference  to  the  present  schistose 
structure  of  the  rock,  and  evidently  represent  original  constituents  of 
the  rock  from  which  the  present  schist  has  been  derived. 

In  place  of  the  above-described  transition  from  massive  to  schistose 
rocks  along  a line — normal  to  the  strike — there  is  in  many  instances  the 
st-ill  more  conclusive  proof  to  be  found  in  this  same  transition  around 
ellipsoidal  or  lenticular  cores  of  massive  rocks.  Such  masses  grow  grad- 
ually schistose  around  their  periphery  and  pass  into  schists  which  ap- 


Williams.]  SCHISTOSE  LAYERS  SURROUNDING  MASSIVE  CORES. 


93 


pear  to  wind  around  and  enclose  them,  but  which,  in  reality,  have  been 
formed  out  of  their  own  substauce.  An  admirable  example  may  be 
seen  just  at  the  Wisconsin  edge  of  the  river  at  the  foot  of  Lower  Quin- 
nesec  Falls.  This  is  a lenticular  mass  of  massive  greenstone  about  eight 
feet  in  its  longest  diameter.  This  grades  insensibly  around  its  edge, 
into  dark  green  schists,  differing  only  in  their  structure  from  the  cen- 
tral rock.  Four  specimens  (Nos.  11017,  11018,  11019,  and  11020)  were 
collected  to  illustrate  this  passage.  The  most  interior  and  massive  one 
(No.  11017),  although  to  all  appearances  quite  compact,  is  found  upon  a 
microscopic  examination  to  be  wholly  altered  mineralogically.  The 
bisilicate  constituents  are  now  represented  only  by  a light  emerald- 
green,  pleochroic  mineral,  which,  in  spite  ot  its  comparatively  strong 
action  upon  polarized  light,  is  probably  chlorite.  This  frequently  con- 
tains sharp  epidote  crystals.  The  feldspar,  while  retaining  much  of  its 
original  form,  is  composed  either  of  a gray,  opaque  saussurite  or  of  a 
fine  mosaic  of  quartz  and  albite  grains  and  a great  deal  of  calcite. 

The  extremely  altered  condition  of  the  central  portion  of  this  core  is 
perhaps  rather  advantageous  than  otherwise,  for,  while  there  can  be  no 
doubt  as  to  its  original  character,  the  transition  to  the  schists  is  seen  to 
take  place  wholly  by  a change  in  structure,  without  further  mineral- 
ogical  alteration. 

No.  11018,  taken  from  a place  where  indications  of  a schistose  structure 
are  already  quite  apparent,  shows  just  the  same  mineral  components  as 
the  last.  The  chlorite  scales,  however,  have  assumed  a decidedly  par- 
allel arrangement,  which  is  followed,  to  a less  extent,  by  the  fine  mosaic 
of  quartz  and  albite  grains.  The  calcite  is  better  crystallized,  and  forms 
larger  individuals.  There  are  also  present  some  minute  scales  of  a deep 
red  iron  oxide,  probably  gothite,  or  limonite.  The  gray  saussurite  is 
likewise  common. 

No.  11019,  in  which  the  schistose  structure  is  still  more  apparent, 
shows  the  same  components  as  the  others.  The  parallel  arrangement 
of  the  chlorite  is  still  more  pronounced  and  the  calcite  still  better  crys- 
tallized. Strangely  enough,  we  meet  here,  in  a very  schistose  rock, 
better  preserved  feldspar  crystals  than  can  be  found  in  the  more  massive 
greenstone,  with  which  it  is  so  intimately  connected.  This  is  but  one 
more  instance  of  the  remarkable  rule  set  down  on  p.  88,  and  alluded 
to  several  times  already.  This  thin  section  (No.  11019)  exhibits  feldspars 
so  well  preserved  that  only  occasional  epidote  crystals  are  developed 
in  them.  There  is  also  to  be  seen  a remarkably  good  example  of  the 
change  of  pyrite  to  iron  hydroxide. 

No.  11020  represents  the  extreme  member  of  this  series.  It  is  a typical 
chlorite  schist,  in  which  alternating  and  interlacing  areas  of  pale  green 
chlorite  and  a fine  quartz  albite  mosaic  may  be  seen.  In  both  a highly 
developed  schistosity  is  produced  by  the  parallel  arrangement  of  the 
components.  The  grain  of  this  rock,  in  so  far  as  it  is  due  to  these  alter- 
nating areas,  appears  somewhat  coarser  than  in  the  less  altered  forms* 


94 


GREENSTONE  SCHIST  AREAS  OF  MICHIGAN. 


[PULL.  63. 


The  chlorite,  if  it  be  examined  with  a higher  magnifying  power,  is  seen 
to  be  filled  with  irregular  spots  of  a reddish  brown  color,  which  feebly 
polarize,  and  seem  to  be  the  remains  of  former  feldspar  crystals.  Rutile 
in  grains  or  sharp  crystal  forms  is  also  present. 

The  fine  mosaic  which  composes  the  other  areas,  contains,  in  addi- 
tion to  the  quartz  and  albite  grains,  calcite  and  chlorite  in  small,  elon- 
gated scales. 

A careful  field  examination  shows  conclusively  that  the  four  speci- 
mens here  described  (Nos.  11017  to  11020),  represent  only  different 
forms  of  the  same  rock.  In  fact,  the  mineral  composition  is  identical 
for  all,  although  the  most  massive  form  is  beyond  all  doubt  an  altered 
diabase,  while  the  exterior  bands,  which  surround  this  core  are  just  as 
truly  examples  of  a typical  chlorite  schist. 

No.  11048  is  a specimen  of  the  massive,  dark  green  rock  which  has 
been  blasted  out  behind  the  shanty  on  the  Michigan  side  of  Lower 
Quinnesec  Falls.  A microscopic  examination  shows  at  once  that  this 
rock  was  originally  a diabase,  although  its  present  constituents  are 
for  the  most  part  secondary.  The  shapes  of  the  original  minerals  are 
indistinctly  outlined,  and  so  the  structure  of  the  rock  is  preserved. 
There  is  now  present  a pale  green  hornblende,  probably  secondary  to 
pyroxene,  although  no  traces  of  this  mineral  are  preserved  ; epidote, 
chlorite,  saussurite  and  leucoxene  in  zones  around  the  titanic  iron. 
The  feldspar  has  rarely  changed  to  the  opaque,  gray  saussurite,  but  is 
replaced  for  the  most  part  by  a mass  of  sharply  defined  epidote  crys- 
tals. Where  the  feldspar  and  hornblende  have  jointly  contributed  to 
the  formation  of  secondary  products,  we  have  the  chlorite  epidote 
aggregate  as  a result.  A little  secondary  quartz  is  also  observable. 

The  two  remaining  specimens  examined  from  Lower  Quinnesec  Falls 
(Nos.  11101  and  11102)  were  collected  on  the  Michigan  side  of  the  river 
above  the  fall,  from  two  xmints  designated  by  u and  w respectively  on 
Major  Brooks’s  map.  They  exhibit  in  a marked  degree  the  effects  of 
stretching  upon  massive  greenstones.  If  a rock  mass  were  subjected 
to  a great  lateral  pressure  when  it  was  free  to  expand  in  a direction 
perpendicular  to  that  in  which  the  pressure  acted,  it  would  appear  as 
though  it  had  been  subjected  to  a strain  or  tension  in  the  direction  along 
which  it  was  free  to  move.  There  would  be  a breaking  and  pulling  out 
of  the  individual  minerals  into  parallel  bands  along  the  line  of  expan- 
sion or  apparent  stretching.  This  phenomenon  is  very  admirably  dis- 
played in  these  two  specimens. 

No.  11102  is  the  coarser  grained  of  the  two  rocks  and  shows  its  struct- 
ure best  when  the  microscopic  section  is  examined  with  a pocket-lens. 
Its  appearance,  as  seen  under  a low  power  of  the  microscope,  is  por- 
trayed in  PL  XI,  fig.  2.  One  of  the  most  important  of  the  original 
constituents  of  this  rock  was  a triclinic  feldspar  in  large  sized  indi- 
viduals. These  are  now  fissured  in  a direction  normal  to  the  stretch- 
ing and  their  fragments  are  separated  in  a most  striking  manner.  The 


williams.]  STRETCHING  OF  ILMENITE  IN  GREENSTONE.  95 

interstices  are  filled  with  long,  chlorite  scales  arranged  perpendicular 
to  the  walls  of  the  fissures,*  more  rarely  calcite  replaces  this  chlorite. 
Here  again  we  have  clear  evidence  that  the  chemical  change  in  the 
feldspars  of  rocks  which  have  been  subjected  to  great  mechanical  action, 
is  comparatively  slight.  The  feldspars  of  this  rock  are  scarcely  altered 
except  by  being  broken  or  crushed. 

The  grains  of  original  quartz  in  this  rock  have  suffered  the  usual  de- 
formation, being  rarely  brokeu  but  more  frequently  in  a state  of  ten- 
sion which  imparts  to  them  an  undulatorv  extinction. 

Very  finely  fibrous,  dark  green  aetinolite  is  quite  abundant,  repre- 
senting some  other  bisilicate  constituent  (either  pyroxene  or  compact 
hornblende)  all  traces  of  which  have  now  disappeared.  The  fibers  are 
sometimes  parallel  over  considerable  areas,  sometimes  crowded  together 
into  a confused  and  matted  mass.  They  themselves  show  no  evidence 
of  pressure  and  hence  must  have  originated  during  the  action  of  the 
pressure  or  subsequent  to  it.  The  former  is  the  more  probable  and  the 
pressure  may  have  been  the  very  cause  to  which  the  hornblende  owes 
its  origin,  as  I suggested  in  a former  paper.1 

None  of  the  constituents  displays  the  effects  of  the  stretching  action 
to  which  this  rock  has  been  subjected  more  distinctly  than  the  ilmen- 
ite.  This  mineral  is  abundant  in  grains  of  considerable  size,  all  of 
which  have  been  irregularly  fissured  in  a direction  transverse  to  the 
tension  and  the  fragments  separated,  exactly  like  those  of  the  feldspar.2 
(See  PI.  XI,  fig.  2.)  The  absence  of  leucoxene  around  these  grains  may 
indicate  that  in  this  case  also  the  chemical  action  is  inversely  propor- 
tional to  the  mechanical. 

No.  1X101  is  a very  similar  rock  of  a finer  grain,  in  which  the  effects 
of  stretching  are  not  so  apparent.  We  therefore  find  the  chemical  al- 
teration of  the  feldspar  proportionately  greater.  This  mineral  is  not 
so  much  broken  as  in  the  specimen  last  described,  but  it  is  filled  with 
secondary  crystallizations  of  chlorite  and  epidote.  The  ilrneuite  is 
broken  and  stretched  in  the  manner  described  in  the  preceding  speci- 
men, though  to  a less  degree.  The  separated  ilmenite  fragments,  how- 
ever, in  this  case  present  a contrast  to  the  others,  in  having  leucoxene 
quite  abundantly  developed  around  them.  The  hornblende  of  this 
rock  is  both  brown  and  green ; each  variety  is  dark  colored  and  in- 
tensely pleochroic.  Most  of  it  is  fibrous,  the  fibers  following  in  their 
arrangement  the  general  direction  of  the  foliation. 

1 Am.  Jour.  Sci.,  3d  Berios,  Oct.,  1884,  vol.  28,  p.  266. 

2A.  Schenck  describes  and  figures  exactly  this  phenomenon  in  the  schistose  diabases  of  the  upper 
Kuhr  Valley.  Inaugural  Dissertation,  Bonn,  1884,  p.  55. 


CHAPTER  III. 


GREENSTONE  BELTS  OF  THE  MENOMINEE  DISTRICT— (Continued). 

UPPER  OR  BIG  QUINNESEC  FALLS. 

About  3J  miles  above  Lower  Quinnesec  Falls,  described  in  the 
preceding  chapter,  the  course  of  the  Menominee  River  is  again 
interrupted  by  extensive  rock  exposures,  which  skirt  the  banks  for 
nearly  2 miles.  The  upper  mile  of  this  distance  is  a high,  rocky  gorge, 
known  as  the  u Horse  Race,”  through  which  the  water  rushes  and 
tumbles  in  a foaming  rapid.  The  current  then  flows  more  quietly 
through  a broader,  though  still  rocky  channel,  for  half  a mile,  when 
it  suddenly  plunges  over  a fall  of  considerable  height  and  beauty,  known 
as  Upper  or  Big  Quinnesec.1 

Below  this  fall  the  stream  broadens  into  a wide  basin,  which  is  also 
bordered  by  rocky  shores. 

The  continuous  exposure  of  Upper  Quinnesec  Falls  is,  therefore, 
separable  into  three  naturally  distinct  divisions.  These  divisions  are, 
moreover,  each  characterized  by  a different  kind  of  rock ; a fact  which 
serves  to  distinguish  them  almost  as  sharply  as  their  physical  confor- 
mation. (See  map,  PI.  Y.) 

The  rocks  which  are  exposed  along  the  basin  belong,  for  the  most 
part,  to  the  class  of  dark,  more  or  less  schistose  greenstones,  similar  to 
those  occurring  at  Lower  Quinnesec  Falls.  These  were  once  diabases 
rich  in  iron,  which  have  produced  amphibolitic  and  chloritic  schists  of 
a deep  green  color. 

The  actual  barrier  at  Upper  Quinnesec  Falls  is,  on  the  other  hand,  com- 
posed of  the  light  colored  type  of  greenstone  with  a distinctly  granular 
structure,  like  that  already  described  as  occurring  at  both  the  Sturgeon 
and  Lower  Quinnesec  Falls.  This  is  also  the  commonest  rock  for  the 
half  mile  above  the  falls,  before  the  rapid  is  reached.  It  is  deserving 
of  careful  study  on  account  of  the  transition  which  it  presents  into 
light  colored  sericite  schists. 

The  rock  which  forms  the  steep  walls  of  the  gorge  known  as  the  Horse 
Race  is  of  still  a different  type.  It  will  receive  a separate  treatment, 
as  it  is  quite  unlike  anything  observed  elsewhere  in  the  Menominee 
Valley. 

1 This  name  is  a corruption  of  the  Chippewa  Bequenesec  which  is  spoiled  by  H.  Credner  in  his  descrip- 
tion of  this  locality  as  Bekuenesek.  (Neues  Jahrbuch  fur  Mineral.,  1870,  p.  971.) 

96 


u.  s.  geological  survey 


BULLETIN  NO.  82  PL.  V 


Schistose  1 


fHt  UWM« 

Of  fHt 


williams.]  GREENSTONES  BELOW  UPPER  QUINNESEC1  FALLS 


97 


Finally  bands  of  certain  acid  rocks— granites,  gneisses,  and  schistose 
porphyries — occur  in  the  greenstones  both  at  the  fall  and  along  the 
Horse  Race.  They  appear  to  stand  in  the  closest  genetic  relation  both 
to  each  other  and  to  the  great  granite  area  which  lies  south  of  the  river 
and  approaches  it  at  this  point  more  nearly  than  at  any  other. 

We  may,  therefore,  consider  the  rocks  of  Upper  or  Big  Quinnesec 
Falls  under  the  four  following  heads: 

(1)  The  dark  colored  greenstones  of  the  basin. 

(2)  The  light  colored  greenstones  at  the  falls. 

(3)  The  coarse  grained  diorites  of  the  Horse  Race. 

(4)  The  acid  rocks,  both  massive  and  schistose. 

THE  DARK  COLORED  GREENSTONES  OF  THE  BASIN. 

At  the  lower  (eastern)  extremity  of  the  basin,  below  Upper  Quinnesec 
Falls,  is  an  exposure  of  greenstone  which  juts  into  the  river  from  the 
Wisconsin  side.  It  is  of  a uniformly  green  color  and,  for  the  most  part, 
massive,  although  schistose  portions  are  not  infrequent,  which  have  the 
X>revailing  strike,  N.  70°  W.,  and  stand  nearly  vertical.  These  schist- 
ose bands  have  in  the  field  every  appearance  of  being  secondary 
since  they  are  only  locally  developed  and  grade  imperceptibly  into 
the  massive  rock.  A specimen  from  this  locality,  No.  11049,  when  ex- 
amined microscopically,  appears  to  be  very  similar  to  a rock  already 
described  from  the  Lower  Falls  (No.  11048).  The  process  of  alteration 
there  indicated,  however,  has  here  progressed  much  further.  There  is 
every  reason  to  believe  that  this  rock,  like  the  other,  was  once  a diabase; 
and  yet,  in  this  case,  all  traces  both  of  the  original  structure  and  of  the 
original  constituents  have  disappeared.  The  feldspar  substance  is  com- 
pletely replaced  by  a confused  network  of  epidote  needles,  or  of  these 
mixed  with  chlorite;  some  rather  compact,  green  hornblende  still  re- 
mains, but  this  mineral  is  rapidly  disappearing,  and  the  manner  in 
which,  jointly  with  the  feldspar,  it  furnishes  the  materials  out  of  which 
the  chlorite-epidote  aggregate  is  formed  is  here  very  instructively  dis- 
played. In  fact,  no  other  rock  showed  this  characteristic  form  of  altera- 
tion as  well  as  this  one,  and  it  was  therefore  selected  to  furnish  the 
illustration.  (See  PI.  XI,  fig.  1.)  The  titanic  iron  is  here  in  the  form  of 
small  grains,  accompanied  by  leucoxene.1 

On  the  southern  or  Wisconsin  side  of  this  basin  there  are  no  more 
important  exposures  of  the  dark  colored  greenstones.  On  the  Mich- 
igan side,  however,  such  exposures  are  abundant  and  have  been  in- 
dicated on  Maj.  Brooks’s  map  as  the  points  0,  au,  bb , and  cc.2 

Two  suites  of  specimens  collected  at  these  points,  one  by  Prof.  Irving 

1 Slide  No.  931  of  the  collection  of  the  Lake  Superior  Division  of  the  U.  S.  Geological  Survey  was 
prepared  from  a specimen  collected  by  Prof.  It.  D.  Irving  west  of  the  above,  among  the  light  colorod 
greenstones.  It  is  of  great  interest  in  this  connection  because  its  feldspar  is  quite  well  preserved  and 
shows  in  a most  unmistakable  manner  the  ophitic  structure  of  tho  diabases.  In  other  respects  espec- 
ially in  the  character  and  abundance  of  the  epidote-chlorite  aggregate,  it  is  quite  identical  with  No. 
11049. 

aGeol.  Wisconsin,  vol.  3,  PI.  3,  p.  474,  • 

Bull  62 7 


98 


GREENSTONE  SCHIST  AREAS  OF  MICHIGAN. 


•[BULL.  62. 


and  the  other  by  the  writer,  were  studied.  The  rocks  all  exhibit  the 
effects  of  extreme  mechanical  action  upon  their  constituents,  which  has 
so  far  obliterated  their  original  structure  as  to  render  their  true  char- 
acter doubtful.  They  agree  in  being  composed  of  different  proportions 
of  a much  crushed  and  altered,  reddish  brown  feldspar  and  a pale  green 
mass  consisting  of  chlorite  aud  quartz.  The  latter  aggregate  is  of  sec- 
ondary origin  and  imparts  a cleavage  to  the  rock,  since  the  chlorite 
flakes  are  all  arranged  in  one  direction. 

No.  4162,  from  Prof.  Irving’s  collection,  was  the  only  specimen  studied 
microscopically  from  poiut  z.  It  is  composed  mostly  of  feldspar,  and 
has,  therefore,  a reddish  color.  This  constituent  is  intensely  crushed 
and  its  substance  is  so  highly  altered  as  to  appear  to  grade  imperceptibly 
into  the  quartz  chlorite  matrix,  which  is  present  in  small  amount  be- 
tween its  fragments.  Scattered  through  this  mass  in  the  direction  of 
its  foliation  are  long  lines  of  some  opaque  iron  oxide,  accompanied  by 
very  minute  though  sharply  defined  crystals  and  twins  of  rutile  (Thon- 
schiefernadeln),  like  those  represented  in  Fig.  12,  p.  106.  In  some  cases 
the  iron  oxide  is  absent,  and  these  dark  bauds  may  be  seen  with  a high 
magnifying  power  to  be  made  up  entirely  of  the  closely  clustered  rutile 
crystals. 

Nos.  4163  aud  11070  are  both  from  Brooks’s  poiut  aa,  which  he  de- 
scribes (loc.  cit.)  as  composed  of  a u chloritic  greenstone  schist,  with 
pinkish  grains  of  feldspar  (Schalstein?).” 

The  first  of  these  sections  belongs  to  Professor  Irving’s  collection, 
and  exhibits  under  the  microscope  the  effects  of  the  crushing  aud 
stretching  in  a very  marked  degree.  Its  structure  resembles  that  of 
specimen  No.  11102  from  the  lower  Quinnesec  Fall,  described  on  p.  94", 
and  represented  in  PI.  XI,  fig  1.  White  and  reddish  feldspar  crystals, 
quartz  grains,  and  opaque  black  spots  of  iron  oxide  are  imbedded  in  a 
secondary  matrix  consisting  of  chlorite,  quartz,  and  epidote.  No  trace 
of  an  original  bisilicate  now  remains.  All  of  the  older  components, 
especially  the  feldspar  and  iron  oxide,  are  much  broken  and  their  frag- 
ments are  separated  in  one  uniform  direction  corresponding  to  the  folia- 
tion of  the  rock ; but  yet  the  fragments  which  once  belonged  together 
can  still  be  recognized.  The  feldspar  substance,  in  spite  of  the  in- 
tense crushing,  is  still  remarkably  fresh  and  its  twinning  striatiou  dis- 
tinct. Lath-shaped  forms,  like  those  of  diabase,  are  present,  though  all 
traces  of  the  original  rock  structure  have  disappeared.  The  opaque 
grains  of  iron  oxide  (magnetite)  are  broken  aud  pulled  apart  like  the 
feldspar  and  can  be  seen  with  a high  magnifying  power  to  be  fringed 
with  minute  and  imperfectly  formed  rutile  crystals.  Sharply  defined 
octabedra  of  magnetite — evidently  of  secondary  origin,  as  they  never 
exhibit  any  traces  of  mechanical  action — are  also  scattered  through 
the  chlorite,  and  in  some  cases  these  octahedra  are  crowded  together 
with  little  rutile  crystals,  both  looking  as  though  they  had  resulted  from 
the  alteration  of  some  ineexistiug  mineral. 


WILLIAMS.] 


RUTILE  IN  ALTERED  DIABASE. 


!)!) 

No.  11070,  collected  by  the  writer  from  the  .same  locality  as  the  last 
(Brooks’s  point  aa ),  possesses  a similar  character,  though  with  -certain 
important  differences.  The  hand-specimen  is  dark  green  in  color  and 
decidedly  schistose.  Under  the  microscope  it  is  seen  to  he  essentially 
the  same  rock  as  that  last  described,  but  in  an  even  more  advanced 
stage  of  alteration.  The  fragments  of  reddish  feldspar,  which  can  still 
be  seen  to  belong  together,  are  here,  as  before,  separated  in  the  direction 
of  the  foliation,  while  the  spaces  between  them  are  filled  with  chlorite 
flakes  and  quartz  grains.  The  feature  of  particular  interest  in  this  speci- 
men is,  however,  the  abundance  of  its  rutile  and  the  constant  and  close 
association  of  this  mineral  with  the  black  iron  oxide.  This  association, 
as  well  as  the  general  appearance  of  this  rock  under  the  microscope, 
is  represented  in  PI.  XIII,  fig.  2.  The  opaque,  black  grains,  which  in 
reflected  light  can  be  seen  to  be  intergrown  with  a considerable  propor- 
tion of  pyrite,  are  surrounded  by  a border  of  stout,  brownish  yellow 
needles,  averaging  from  0.1  to  0.05 mm  in  length  by  from  0.02  to  0.01mm 
in  width.  They  are  crowded  closely  together  and  are  often  parallel  to 
the  external  edges  of  the  grains.  Xot  infrequently,  also,  they  exhibit 
a regularity  of  arrangement,  crossing  each  other  at  angles  approaching 
60°  and  120°.  It  will  be  readily  seen,  however,  that  in  a random  sec- 
tion of  the  rock  it  is  impossible  to  decide  whether  these  are  exactly  the 
angles  or  whether  they  are  the  angles  54°  43'  and  65°  35'  (with  their 
supplements,  125°  17'  and  114°  25'),  which  von  Lasaulx  has  shown  are 
produced  by  the  twinning  of  rutile,  and  characteristic  of  its  network 
growth  called  as  sagenite.1  An  isolation  of  these  needles  was  made  by 
dissolving  all  the  other  constituents  of  the  rock  in  HOI  and  HF,  for 
the  purpose  of  obtaining  material  which  might  positively  decide  this 
point,  but  no  definite  results  were  obtained.  The  needles  are  for  the  most 
part  irregular  in  their  arrangement,  and  it  still  remains  uncertain  whether 
their  occasional  regularity  is  due  to  twinning  or  to  some  other  cause. 

A chemical  examination  of  the  isolated  needles  showed  that  they  were 
composed  of  titanium  oxide,  while  their  crystallographic  and  optical 
properties  observed  under  the  microscope  proved  them  to  belong  to  the 
species  rutile. 

The  fact  that  the  black,  opaque  constituent  of  this  rock  is  traversed 
by  parallel  cracks  and  fissures,  often  in  sets  intersecting  at  an  angle  df 
60°,  like  those  observed  in  titanic  iron,  taken  in  connection  with  the 
close  relationship  of  the  rock  itself  to  the  family  of  diabases,  naturally 
led  to  the  assumption  that  the  iron  oxide  was  ilraenite.  Moreover,  the 
similarity  of  the  distribution  of  the  rutile  about  the  black  cores  to  that 
of  leucoxene  about  ilmenite  crystals  in  the  process  of  alteration — its 
presence  its  a continuous  border  and  in  every  crack,  while  the  black 
substance  itself  is  quite  free  from  the  needles 2 — seemed  further  to  iudi- 

1 Zoitschr.  fur  Kryst.  u.  Miu.,  vol.  8,  1384,  p.  56. 

2This  was  shown,  not  merely  by  the  absence  of  the  larger  needlos  which,  if  they  wore  present, 
must  have  appeared  through  the  black  substance  of  the  iron  oxido  in  the  thin  section,  but  also  by 
slowly  dissolving  away  the  oxide  with  HC1  under  tho  microscope  and  the  failure  thus  to  discloso  any 
Smaller  crystals  ot  rutile,  which  might  have  been  wholly  inclosed  within  the  black  ore. 


100  GREENSTONE  SCHIST  AREAS  OF  MICHIGAN.  | bull.  62. 

cate  the  secondary  origin  of  the  rutile  out  of  the  ilmenite.  This  is  the 
view  that  was  at  first  taken  by  the  writer  and  published  by  him  in  a 
letter  to  the  Neues  Jahrbuch  fur  Mineralogie,  etc.,  1887,  vol.  2,  p. 
203.  In  a subsequent  paper  on  the  same  rock,1  Prof.  Oathrein  of  Karls- 
ruhe showed,  among  other  points  which  he  considered  as  objec- 
tions to  the  secondary  origin  of  the  rutile,  that  the  black  iron  oxide 
was  not  ilmenite  at  all,  but  magnetite.  This  determination  has  since 
been  confirmed  by  a careful  chemical  examination  made  at  my  request 
by  Prof.  S.  L.  Penfield,  of  the  Sheffield  Scientific  School  at  New  Haven. 

A very  similar  occurrence  of  rutile  needles,  though  inferior  in  size  to 
those  here  described,  has  been  observed  by  Oathrein  in  the  leucoxeue  1 
border  which  surrounds  both  ilmenite2  and  titaniferous  magnetite3  in 
certain  Tyrolese  rocks.  Dr.  J.  Blaas  also  encountered  the  same  kind 
of  a network  of  rutile  crystals  in  a quartz  phyllite  from  the  neighbor- 
hood of  Innsbruck,  but  in  this  case  it  was  unaccompanied  by  any  opaque 
ore.4  In  none  of  the  instances  observed  by  him  does  Oathrein  consider  - 
the  rutile  as  even  possibly  a secondary  product.  On  the  other  hand, 
he  thinks  that  the  little  needles  were  formed  simultaneously  with  the 
ilmenite  or  magnetite,  and  that  they  have  always  existed  in  their  pres- 
ent form  within  the  iron  oxide,  until  more  or  less  completely  liberated 
by  the  solution  and  removal  of  the  latter. 

In  his  article  on  the  Quinnesee  rock  above  cited,  none  of  the  points 
insisted  upon  by  Oathrein  appear  to  militate  against  the  secondary  origin 
of  the  rutile,  except  the  last.  As  has  been  stated  above,  it  is  impossi- 
ble in  a random  section  to  determine  with  certainty  whether  the  nee-  : 
dies  intersect  at  angles  of  exactly  G0°  and  120°,  or  at  those  so  nearly 
like  them  produced  by  twinning.  But  whichever  be  true,  it  is  certain  5 
that  a large  majority  of  the  needles  are  quite  irregular  in  their  arrange- 
ment. The  discovery,  however,  that  the  black  iron  oxide  which  ac- 
companies the  rutile  is  not  ilmenite  but  a magnetite  almost  free  from  ' 
titanium,  seems  at  first  altogether  incompatible  with  the  idea  that  the 
rutile  is  a secondary  derivative  from  ilmenite.  Nevertheless,  a continued 
and  repeated  study  of  a large  number  of  thin  sections  of  this  rock  have  , 
served  to  convince  the  writer  more  and  more  that  the  rutile  was  at 
least  not  a constituent  of  the  rock  in  its  original  state.  The  rutile  ag- 
gregates are  never  drawn  out  in  the  direction  of  the  stretching,  as  are 
all  of  the  original  constituents,  notably  the  feldspar,  and  as  they  must 
have  been  had  they  always  been  present  in  the  rock.  It  is  necessary,  " 
therefore,  to  assume  that  they  originated  subsequent  to,  or,  more  prob- 
ably, at  the  time  of  the  metamorphism. 

The  constant  and  intimate  connection  between  the  rutile  and  the 
magnetite  clearly  shows  that  they  are  in  some  way  genetically  related. 
Opposed  to  the  supposition  that  they  were  originally  parallel  inter- 

1 Neues  Jahrbuch  fur  Mineral.,  etc.,  1888,  vol.  2,  pp.  151-165. 

2Zeitschr.  fur  Kryst.  u.  Miu.,  vol.  6,  1882,  p.  248. 

3 Ibid.,  vol.  8,  1884,  p.  321. 

4 Tschormak’s  min.  u.  petrog.  Mittheil,,  vol.  4,  1882,  p.  514,  fig.  2. 


. 


— 


WILLIAMS.] 


PROBABLE  ORIGIN  OP  THE  RUTILE. 


101 


growths,  is,  however,  the  fact  that  the  rutile  needles  never  occur  within 
the  magnetite,  now  present.  The  rutile  forms  a border  around  the  black 
areas,  which  themselves  frequently  show  a sharp  crystal  outline,  diffi- 
cult to  reconcile  with  the  idea  that  they  have  been  partially  dissolved 
so  as  to  reveal  the  rutile  which  once  existed  within  them.  In  one  in- 
stance, indeed,  an  aggregate  consisting  of  rutile  needles  and  sharp  oc- 
tahedra  of  magnetite  was  observed,  but  this  is  exceptional.  On  the 
other  hand,  it  may  often  be  clearly  seen  that  the  magnetite  has,  to  a 
greater  or  less  degree,  been  removed  by  solution ; but  in  all  such  cases 
the  place  that  it  once  occupied  exists  within  the  fringe  of  rutile,  but  is 
itself  wholly  free  from  the  needles.  This  space  is  often  filled  with  cal- 
cite,  or  some  similar  carbonate,  in  slightly  radiating  tufts. 

All  of  these  observations  seem  to  point  to  a contemporary  origin  for 
both  the  magnetite  and  rutile  from  some  preexisting  mineral,  which  in 
the  present  case  may  very  probably  have  been  ilmenite. 

The  change  of  hematite  into  magnetite  is  one  which  has  been  often 
observed.  Roth 1 quotes  descriptions  of  this  alteration  from  Breithaupt, 
Volger,  Peters,  vom  Rath,  Petersen,  Doll,  Grattarola,  and  Zeparovich. 
There  seems  to  be  no  reason  why  the  corresponding  titaniferous  com- 
pound, ilmenite,  should  not  also  pass  over  into  magnetite  with  the 
separation  of  its  titanium  in  the  form  which  is  most  stable  for  the  con- 
ditions then  prevailing. 

Rutile  is  well  known  to  be  widely  distributed  in  microscopic  crystals 
through  schists  which  have  resulted  from  the  regional  metamorphism 
of  both  sedimentary  and  eruptive  rocks.  It  must  therefore  be  a com- 
pound well  in  accord  with  the  conditions  producing  metamorphism. 

The  common  presence  of  rutile  needles  in  diabase  rocks  which  have 
been  intensely  altered  by  pressure,  and  its  absence  in  their  unaltered 
forms,  in  connection  with  the  fact  that  the  original  ilmenite  disappears 
in  proportion  as  the  rutile  is  developed,  has  inclined  such  eminent 
petrographers  as  Lossen  and  Rosenbusch  to  the  supposition  that  the 
latter  mineral  has  originated  from  an  alteration  of  the  former.  This 
hypothesis  has  derived  much  support  from  observations  made  in  many 
of  the  Lake  Superior  greenstone  schists  which  are  altered  diabases. 
In  case  of  the  particular  rock  under  discussion,  it  is  impossible  to 
prove  with  the  material  now  in  hand  that  the  magnetite  and  associated 
rutile  have  resulted  from  preexisting  ilmenite,  but  in  light  of  all  that 
we  know  of  this  and  other  occurrences,  it  seems  to  the  wrriter  that  sucli 
an  origin  is,  to  say  the  least,  not  at  all  improbable.  Whether  or  not 
such  an  alteration  as  that  here  suggested  really  takes  place  in  the 
ilmenite  of  diabase  when  this  rock  undergoes  dynamic  metamorphism 
to  chloritic  schists  must  remain  for  future  investigations  to  decide. 

Eos.  4164  and  4105,  from  Prof.  Irving’s  collection,  show  the  same 
rock  as  the  two  specimens  last  described  in  a yet  more  advanced  stage 
of  alteration.  Both  have  become  typical  chlorite  schists,  composed 


1 Allgomeino  un<l  chomischo  Geologic,  vol.  1,  1879,  p.  97. 


102 


GREENSTONE  SCHIST  AREAS  OB'  MICHIGAN. 


[BULL-  62. 


mostly  of  chlorite,  quartz,  and  iron  hydroxide.  The  structure  is  now 
finely  parallel  and  schistose,  not  the  least  trace  of  the  original  structure 
remaining.  In  No.  4165,  which  is  the  darker  colored  of  the  two,  leaf- 
lets of  a colorless  mica  (sericite)  are  abundant. 

No.  11072,  collected  from  Brooks’s  point  cc,  is  a dark  green  rock,  which 
is  seen  with  the  unaided  eye  to  be  traversed  by  numerous  fibrous  veins 
of  a paler  green  color.  Under  the  microscope  the  section  of  this  rock 
shows  principally  ragged  areas  of  green  hornblende,  inclosing  isolated 
crystals  of  a mineral,  which  agrees  more  closely  in  its  physical  proper- 
ties with  zoisite  than  with  any  other;  i.  e.,  there  are  colorless  rectan- 
gular sections  with  a cleavage  parallel  to  the  longest  axis,  and  a cross- 
parting in  the  direction  perpendicular  to  this.  In  polarized  light  these 
sections  show  pale,  bluish  gray  interference  colors,  parallel  extinction, 
and  a biaxial  figure.  The  fibrous  veins,  which  compose  a considerable 
proportion  of  the  rock,  are  made  up  of  zoisite  individuals  arranged 
perpendicular  to  the  walls  of  the  vein,  and  of  fibrous  hornblende,  which 
often  penetrates  the  former  mineral  in  fine  asbestiform  needles. 

THE  LIGHT  COLORED  GREENSTONE  AT  UPPER  QUINNESEC  FALLS. 

The  speckled  rock  which  forms  the  barrier  at  Dpper  Quinnesec  Falls, 
is  a very  typical  representative  of  the  light  colored  greenstones  of  the 
Menominee  region.  It  has  a strong  macroscopical  resemblance  to  the 
rocks  of  this  type  already  described  from  Sturgeon  Falls  and  Lower 
Quinnesec  Falls,  but  is  more  attractive  in  appearance  than  any  of  them. 
In  the  field  it  appears  to  be  a medium  grained  aggregate  of  a white, 
opaque  feldspar,  in  which,  however,  glistening,  striated  surfaces  are  by 
no  means  rare,  and  a grayish  green  mineral  with  a half  metallic  luster 
on  its  cleavage  planes.  The  deceptive  appearance  of  this  mineral  is  the 
reason  why  Prof.  Hermann  Credner  calls  this  rock  (which  he  described 
as  early  as  1870)  a diabase  with  a decided  resemblance  to  a gabbro.1 

This  mineral  does,  indeed,  show  the  most  striking  macroscopical  sim- 
ilarity  to  the  diallage  of  some  of  the  Volpersdorf  and  Italian  gabbros; 
but  in  spite  of  this  fact,  the  most  careful  microscopical  examination  of 
many  different  specimens — the  freshest  that  could  be  discovered — 
failed  to  disclose  a trace  of  pyroxene.  This  result  is  the  more  surpris-  1 
ing  as  the  rock  appears  even  fresher  than  that  at  Sturgeon  Falls  in 
which  considerable  pale  diallage  still  remains.  The  microscope,  how-  ; 
ever,  shows  that  the  rock  at  Upper  Quinnesec  Falls  is  the  more  altered  4 
of  the  two. 

No.  11054,  collected  on  the  Wisconsin  side  of  the  river,  directly  at  J 
the  fall,  may  be  regarded  as  a typical  specimen  of  the  perfectly  massive  3 

1 In  speaking  of  this  constituent  he  says:  “ Er  [dor  Augit]  bihlet  kurzsaukmfbrmige,  zu  krystal-  a 
linischeu  Partion  verwachsene  Individuen,  an  dentin  orthodiagoualo  Spaltungstlachen  mit  halbme?^8 
t allisohem  Glanze  besonders  deutlich  hervortreteu.  Dadurch  erhalt  das  Gestein  eine  Aehnlichkeit  mit  -S 
Gabbro,  selbst  mit  Hypersthonit.”  (Neues  Jahrbuch  l'iir  Mineral.,  1870,  p.  972.)  Professor  Pumpelly  ;1 
also  says  tliat^kis  rock  is  identical  with  that  of  Sturgeon  Falls.  (Geol.  Wisconsin,  Vol.  3,  p.  564.) 


Williams.]  GABBRO-DIORITE  OF  UPPER  QUINNESEC  FALLS. 


103 


rock.  Its  microscopical  appearance  is  represented  in  Plate  X,  tig. 
1.  The  hornblende  is  mostly  of  a very  pale  color  and  more  or  less 
fibrous  in  structure.  It  has  every  appearance  of  being  secondary,  and  yet 
in  every  case  where  it  can  be  traced  into  a more  compact  mineral  this 
is  also  a hornblende  of  a dark  green  or  brown  color.  In  many  instances 
the  hornblende  is  bent  and  curved,  as  diullage  is  so  apt  to  be  (see  right 
side  of  the  plate);  but  the  most  striking  peculiarity  of  this  hornblende 
and  the  one  most  like  diallage  is  its  very  perfect  parting,  parallel  to  the 
orthopinacoid  (100).  This  very  unusual  feature  is  apparently  confined 
to  the  paler,  and  probably  secondary  hornblende.  It  stops  abruptly  on 
the  edge  of  the  compact,  more  deeply  colored  variety,  even  where  this 
is  continuous  with  the  lighter  kind  (Plate  X,  fig.  I).1  This  may  indi- 
cate that  the  paler  hornblende  is  secondary  after  diallage  and  therefore 
reproduces  its  orthopinacoidal  parting,  while  the  diallage  was  itself 
intergrown  with  an  original  compact  hornblende  which  still  remains. 
Aside  from  its  characteristic  prismatic  cleavage,  proof  is  furnished  that 
this  mineral  is  really  hornblende  by  the  fact  that  sections  approximately 
perpendicular  to  the  vertical  axis,  give,  in  converged  polarized  light,  a 
bisectrix  instead  of  an  optical  axis. 

The  feldspar  of  this  rock  is  largely  changed  to  opaque,  gray  saussur- 
ite.  Portions  of  it,  however,  remain  in  an  unaltered  state.  These 
have,  even  in  the  thinest  sections,  a pale  brown  color  (PI.  X,  fig.  1), 
and  in  thicker  sections  they  are  as  dark  as  mahogany.  This  coloring 
is  not  due  to  Inclusions  from  which  the  feldspar  is  surprisingly  free,  but 
to  some  unevenly  distributed  pigment  whose  nature  it  is  far  beyond  the 
power  of  the  microscope  to  reveal.  With  the  exception  of  this  color 
the  feldspar  is  so  remarkably  fresh  and  clear  as  to  make  the  impression 
at  first  glance  that  it  must  be  of  secondary  origin.  A slight  examina- 
tion, however,  shows  that  the  clear  brown  substance  forms  a peripheral 
zone  about  the  saussuritized  individuals  ; or  where  the  whole  crystal  is 
unchanged,  that  it  is  bent,  broken,  or  faulted  in  a manner  inconsistent 
with  any  supposition  of  secondary  origin.  Here  again  we  have  addi- 
tional, and,  indeed,  most  convincing  evidence  that  the  greater  the  me- 
chanical action  to  which  the  feldspar  has  been  subjected,  the  less  chem- 
ical change  it  has  undergone.  (See  above,  p.  88.) 

The  other  constituents  of  this  rock  are  ilmenite,  surrounded  by  a leu- 
coxene  border,  and  some  secondary  quartz,  which  is  penetrated  by  most 
delicate  fibers  of  hornblende. 

The  analysis  of  this  rock  in  column  I of  the  following  table  was  made 
by  Mr.  B.  B.  Iiiggs: 

1 It  is  interesting  to  note,  in  this  connection,  tho  recent  observation  of  Cathrein  that  the  hornblende 
of  Roda  in  the  Tyrol  lias  a perfectly  developed  parting  due  to  very  narrow  twimiing-lamelhe  which  run 
parallel  to  the  orthopinacoid.  (Zeitsclir.  fur  Kryst.  u.  Min.,  vol.  12,  p.  12.)  Whether  tho  above-men- 
tioned parting  is  due  to  the  same  cause  or  not,  it  is  impossible,  on  account  of  tho  extreme  narrowness 

of  the  parting-liDes,  to  determine. 


104  GREENSTONE  SCHIST  AREAS  OF  MICHIGAN.  [bull.  62. 


1 i 

ir. 

j 

Silica  (Si02) 

: 48.35 

51.46 

47.96 

Alumina  (A1203) 

15. 40 

1 14. 35 

I 16.85 

Ferric  oxide  (Fe203) 

4.  04 

3/90 

: 4.33 

Ferrous  oxide  (FeO)..-. - 

4.63 

5.28 

' 4.17 

Lime(CaO) 

10.  38 

9.  08 

13.  25 

Magnesia  (MgO) 

11.61 

9.  54 

9.15 

Soda  (Xa.20) .’. 

1.87 

2. 92 

1.25 

.Potasli  (KaO) 

• 35 

.24 

.30 

Water  (H20) 

3.60 

3. 30 

2.  89 

Carbon  dioxide  (C02) . . . 

.08 

.20 

.08 

Total 

100.31 

100. 27 

! 100.23 

Dried  at  105°. 

The  analyses  of  the  two  analogous  rocks,  Nos.  11171  (II)  from  Sturgeon 
Falls,  and  11008  (III),  from  Lower  Quinnesec  Falls,  are  again  cited  from 
pp.  76  and  89,  for  comparison.  The  agreement  between  all  three  analyses 
is  as  close  as  could  be  expected  for  three  different  specimens  of  the 
same  rockmass.  In  fact  it  is  difficult  to  escape  the  conviction  that  the 
rocks  from  both  Upper  and  Lower  Quinnesec  Falls,  like  that  from  Stur- 
geon Falls,  were  once  diallage-plagioclase  aggregates  or  gabbros  $ and 
yet  if  this  be  true,  we  are  compelled  to  assume  either  that  the  original 
diallage  passed  by  paramorphism  into  compact  brown  hornblende  be- 
fore reaching  its  present  state ; or  that  the  original  rock  was  a horn- 
blende gabbro  in  which  both  bisilicate  constituents  passed  finally  into 
pale  fibrous  hornblende,  although  this  process  progressed  much  more 
slowly  with  the  hornblende  than  with  the  pyroxene. 

The  feldspathic  component  of  this  rock  (No.  11054)  is  determined  by 
the  analysis  to  be  labradorite,  as  was  also  found  to  be  the  case  in  the 
corresponding  specimens  from  the  other  localities. 

Two  other  specimens  of  this  same  rock,  No.  11061,  from  the  Michi- 
gan side  of  the  falls,  and  No.  11073,  from  a point  above  the  falls, 
marked  p on  Major  Brooks’s  map,  are  essentially  the  same  as  the  one 
just  described.  Both  are,  however,  more  altered  and  both  show,  in  a 
still  greater  degree,  the  effects  of  pressure  upon  the  constituent  minerals. 
In  No.  11061  a good  deal  of  quartz  is  present,  always  penetrated  by 
delicate  needles  and  tufts  of  hornblende.  The  largest  areas  of  this 
quartz  form  a rather  coarse  grained  mosaic  and  look  as  though  they 
had  been  deposited  as  a pseudomorph  after  some  former  constituent. 
Some  colorless  chlorite  is  also  present  in  this  section,  having  been  de- 
rived from  the  alteration  of  the  hornblende.  The  feldspar  of  No. 
11073  is  colorless,  and  has  been  fissured,  broken,  and  even  crushed  in  a 
surprising  manner.  As  a result,  the  saussuritization  of  this  mineral  has 
hardly  more  than  commenced,  in  spite  of  the  advanced  state  of  altera- 
tion observable  in  the  hornblende.  One  hornblende  section  in  this 
slide,  cut  nearly  perpendicular  to  the  vertical  axis,  shows  a very  sharp 
line  of  demarcation  between  the  interior,  dark  brown  portion  and  the 


wiluams.]  SHEARED  GABBRO-DIORITE.  105 

colorless  peripheral  zone.  This  resembles  somewhat  the  secondary  horn- 
blende enlargements  recently  described  by  Van  Hise,1  but  I can  not 
regard  this  particular  case  as  due  to  anything  but  exterior  bleaching. 

Nos.  11056  and  11057,  from  the  Wisconsin  side  of  the  fall,  illustrate 
the  passage  of  this  pale  diorite  into  schistose  varieties,  as  described  at 
Lower  Quinnesec  Falls.  The  former  specimen,  though  macroscopicaily 
still  quite  massite,  has  lost  the  distinctness  of  its  structure.  Under  the 
microscope  this  is  seen  to  be  due  to  crushing  and  attendant  chemical 
changes.  The  feldspar  is  almost  pulverized,  but  has  otherwise  un- 
dergone but  little  change.  A few  of  the  larger  crystals  have  been  merely 

cracked  and  faulted  as  shown  in  Fig. 
11.  The  hornblende  is  very  largely 
changed  to  a colorless  chlorite. 
Where  one  of  the  hornblende  crys- 
tals has  been  broken  and  sheared, 
chlorite  is  seen  to  have  been  devel- 
oped in  parallel  fibers.  This  fur- 
nishes an  admirable  microscopic  illus- 
tration of  how  the  schistose  bands 
are  formed  by  pressure  in  the  rock- 
mass  as  a whole.  (See  also  Fig.  22,  p. 
128.)  Just  below  the  falls  this  rock 
becomes  broken,  gashed,  and  seamed 
with  narrow,  paraliel  veins  of  lamel- 
lar minerals.  These  gradually  in- 
crease to  bands,  which  finally  com- 
pose the  main  portion  of  the  rock.  There  can  remain  no  doubt  in  the 
mind  of  anyone  who  will  carefully  study  this  exposure,  that  these  schis- 
tose bands  have  been  produced  in  the  massive  rock  by  the  action  of 
pressure,  along  lines  where  there  has  been  a shearing  motion. 

No.  11057  is  from  one  of  the  schistose  bands  in  No.  11056.  The  micro- 
scope shows  it  to  be  composed  of  a fine  mosaic  of  quartz  and  feldspar  (?) 
grains,  made  schistose  by  parallel  fibers  of  serpentine  and  chlorite. 

At  and  just  below  the  engine  house  on  the  Michigan  side  of  Upper 
Quinnesec.  Falls  is  another  exposure  which  illustrates  the  gradual 
passage  of  these  light  colored,  massive  greenstones,  into  silvery,  hydrous 
schists,  similar  to  those  described  as  occurring  just  below  Lower  Quin- 
nesec Falls. 

No.  11065  is  a very  light  colored,  although  nearly  massive,  rock,  seen 
in  situ  in  a wall  behind  the  engine  house.  It  is  composed  of  much 
crushed  and  faulted  feldspar  of  the  above  described  brown  variety, 
together  with  colorless  isotropic  chlorite.  There  is  also  some  of  the 
quartz  albite  mosaic,  though  this  is  not  abundantly  developed,  with  a 
little  iron  oxide.  There  is  no  parallelism  in  the  arrangement  of  the 
constituents  which  would  tend  to  produce  a schistose  structure. 


Fig.  11. — Faulted  feldspar  crystal  in  crushed 
greenstone  (No.  11056)  from  Upper  Quinnesec 
Falls.  Nicols  crossed ; magnified  30  diame- 
ters. 


1 Am.  Jour.  Sci.,  3d  series  vol.,  33,  1887,  p.  385. 


106  GREENSTONE  SCHIST  AREAS  OF  MICHIGAN.  [bul'l.  62. 

No.  HOGG  is  from  the  same  rock- wall  as  the  last  specimen  and  is  un- 
doubtedly continuous  with  it.  It  is  decidedly  schistose,  and  is  com- 
posed wholly  of  a granular  mosaic,  with  both  sericite  scales  and  a col- 
orless chlorite.  There  are  the  finest  microscopic  rutile  crystals  in  this 

rock  that  were  encountered  in  any 
specim  ens  from  the  Menominee  region . 
These  crystals  are  simple  individuals, 
twins  and  trillings  showing  a great 
variety  of  form.  A few  are  repre- 
sented in  the  accompanying  figure. 
They  are  grouped  together  or  ar- 
ranged in  lines  or  strings  which  fol- 
low the  direction  of  the  schistosity. 
As  in  other  similar  instances  before 
described  from  the  Lower  Falls,  they 
appear  to  have  originated  from  the 
alteration  of  the  ilmenite  of  the  mas- 
sive rock. 

Just  below  the  engine-house  similar 
sericite  schists  are  exposed  (No.  11067  ])  which  contain  green  chlorite  in 
spots  and  appear  to  grade  into  typical  dark  green  chlorite  schists  (No. 
11068).  These  rocks  are  mentioned  by  Major  Brooks  at  the  exposures 
marked  on  his  map  x and  y2.  These  dark  green  schists  are  like  those 
which  originate  from  the  alteration  of  the  dark  colored  diabases,  and 
their  appearance  probably  marks  the  commencement  of  the  belt  of  these 
rocks  which  skirts  the  basin  below  the  Falls. 


Fig.  12.— Ru  tile  needles  in  Xo.  71056  magnified 
350  diameters. 


THE  COARSE  GRAINED  DIORITES  OF  THE  HORSE  RACE. 

The  half  mile  of  comparatively  quiet  water,  navigable  by  a small 
boat  or  canoe,  immediately  above  the  tJ pper  Quinnesec  Falls  is  bordered 
mostly  by  massive  or  schistose  greenstones  of  the  dark  type  similar  in 
all  respects  to  the  rocks  of  this  kind  which  have  been  studied  at  sev- 
eral other  localities  on  the  Menominee  River.  They  are  interspersed 
with  bands  of  gneissose  rock,  identical  with  those  yet  to  be  de- 
scribed. 

The  narrow  gorge  known  as  the  Horse  Race,  through  which  the  river 
flows  for  a mile  or  more,  has,  however,  been  excavated  through  rocks 
of  a quite  different  character.  These  are  for  the  most  part  coarse 
grained  diorites,  penetrated  by  bands  of  granitic  and  gneissic  rocks 
which  will  receive  special  consideration  in  the  following  section. 

Typical  specimens  of  these  coarse  grained  diorites  are  Nos.  11077  and 
11093  from  the  Wisconsin,  and  Nos.  11182,  11183,  11185,  aud  11186 
from  the  Michigan  side  of  the  rapids. 

The  macroscopical  appearance  of  these  rocks  is  often  that  of  an  almost 

‘This  rock  was  called  by  H.  Credner  “ talc-schist ” in  1869  (Zeitschr.  Deutsch.  geol.  Gesell.,  vol. 
21,  p.  529).  It  was  described  in  1876  by  Wichmann,  who  gives  seven  reasons  for  regarding  the  sericite 
schists  as  of  fragmental  origin.  (Geol.  Wisconsin,  vol.  3,  p.  638.) 

2Ibid.,  1,  pp.  473,474. 


williams.]  THE  DIORITES  OF  THE  “ HORSE  RACE.”  107 

uniformly  gray  mass,  in  which  the  large  and  frequently  glistening  horn- 
blende crystals  are  not  at  first  glance  very  apparent.  This  color  is  due 
to  the  alteration  of  the  feldspar,  in  which  new  minerals  are  largely  de- 
veloped. An  opaque,  while  feldspar,  or  rather  saussurite,  is,  however, 
often  visible.  This  is  sometimes  in  the  form  of  rounded  or  oval  areas 
which  represent  the  centers  of  crystals  that  have  turned  gray  around 
their  edges ; sometimes  in  the  form  of  the  original  feldspar  crystals 
themselves,  and  agaiu  in  sharp  contrast  with  the  dark  green  horn- 
blende. The  grain  of  these  rocks  varies  extremely,  but  is  rarely  fine. 
The  form  of  the  different  constituents  is  always  visible  to  the  naked 
eye  ; and,  in  some  instances  (No.  11192),  these  measure  from  one  to 
two  inches  in  diameter. 

Aside  from  the  unusual  coarseness  of  their  grain,  the  rocks  of  the 
Horse  Race  differ  from  the  other  greenstones  of  the  Menominee  in  fre- 
quently containing  biotite.  Another  striking  contrast  is  presented  in 
the  almost  universal  presence  of  talc.  This  mineral  has  without 
doubt  originated  from  the  hornblende,  and  has  wandered  from  it 
into  the  feldspar.  It  is  scattered  everywhere  through  the  rock  in 
minute,  silvery,  glistening  scales,  and  it  coats  all  cracks  and  fissures. 
The  surface  of  the  hornblende  crystals  is  also  frequently  spotted  with 
it.  The  nature  of  this  mineral  as  talc  is  easily  determined  by  both  op- 
tical and  chemical  means.  Under  the  microscope  it  is  of  a pale  green 
color,  resembling  muscovite  in  its  cleavage  and  brilliant  interference 
colors,  but  with  a small  optical  angle  and  negative  character.  It  is 
infusible  and  not  attacked  by  acids,  while  microchemical  tests  show 
that  it  is  destitute  of  both  alumina  and  alkalies. 

The  structure  of  the  Horse  Race  rocks  is  that  of  the  second  kind 
mentioned  by  Rosenbusch  as  occurring  in  diorite,1  i.  e.,  that  conditioned 
by  the  feldspar  having  crystallized  before  the  hornblende.  The  latter 
component  is  plainly  allotrimorphic,  like  the  pyroxene  in  diabase, 
while  the  feldspar  has  a well  developed  form  of  its  own.  (PI.  XII, 
fig.  2.)  The  hornblende,  although  comparatively  compact  and  homo- 
geneous over  considerable  areas,  nevertheless  conveys  the  impression 
of  being  of  secondary  origin.  It  has  a pale  green  color,  slightly  darker 
toward  the  edge,  and  is  externally  frayed  out  into  a fringe  of  radiat- 
ing actinolite  fibers,  which  wander  along  the  cracks  in  the  feldspar. 
(No.  11186;  see  PI.  XII,  fig.  2.)  In  some  sections — notably  in  No. 
11185 — large  portions  of  the  hornblende  have  become  wholly  changed 
to  a felt  like  network  of  minute  fibers.  These  characters,  together 
with  the  shape  of  the  hornblende  individuals,  convey  the  impression 
that  they  have  been  derived  from  pyroxene.  While,  therefore,  it  is 
impossible  to  prove  it  with  certainty,  it  is  difficult  to  escape  the  con- 
viction that  these  rocks  were  originally  coarse  grained  gabbros  or 
diabases. 

The  feldspar  shows  in  almost  every  instance  a broad  twinning  stria- 


Mikroa.  Physiog.,  2d  cd.,  vol.2,  p.  121. 


108 


GREENSTONE  SCHIST  AREAS  OF  MICHIGAN. 


[bull.  62. 


tioii,  although  this  is  more  or  less  obscured  by  chemical  changes.  In 
one  specimen  (No.  11182)  there  is  a brown  feldspar  which  is  perfectly 
preserved  around  the  periphery  of  the  crystals,  while  their  interior  is 
changed  to  saussurite.  In  other  cases  (Nos.  11093  and  11185)  the  feld- 
spar is  largely  changed  to  saussurite,  with  which  is  mingled  a good  deal  of 
actiuolite  and  some  biotite.  In  the  latter  case  clear  areas  of  brilliantly 
polarizing  talc  are  quite  abundant.  In  Nos.  11077  and  11186  the  white 
or  colorless  feldspar  is  comparatively  well  preserved,  but  it  is  filled  with 
pale  green  actinolite  needles  and  some  little  biotite,  which  appear  to 
have  wandered  into  it  from  the  hornblende.  In  these  rocks  the  amount 
of  saussurite  is  inconsiderable. 

Brown  biotite  is  not  infrequently  an  important  constituent  of  these 
rocks.  It  is  especially  abundant  in  No.  11077.  Although  sparingly 
scattered  through  the  feldspar  like  the  actinolite,  it  is  mainly  to  be 
found  in  close  association  with  the  hornblende,  with  which  or  out  of 
which  it  seems  to  have  been  developed  by  secondary  processes. 

Other  specimens  represent  exceptional  varieties  of  the  Horse  Bace 
diorites. 

No.  11091,  from  the  Wisconsin  bank  of  the  stream,  shows  the  feld- 
spar wholly  changed  to  a compact  aggregate  of  epidote  grains.1  The 
hornblende,  which  is  in  sharp  crystals,  presents  its  usual  appearance 
and  characteristics.  The  epidote  is  so  light  colored  that  it  might 
easily  be  mistaken  at  first  glance  for  feldspar  in  the  hand-specimen. 
The  microscope,  however,  at  once  shows  its  true  character.  The  inter- 
ference colors  of  the  closely  interlocking  grains  present  a brilliant 
appearance.  No  trace  of  the  original  feldspar  remains.  Only  an  occa- 
sional grain  of  calcite  or  quartz  interrupts  the  continuity  of  the  epidote. 
Epidote  is  not  an  unusual  secondary  product  in  feldspar,  although  such 
perfect  pseudomorphs  of  this  mineral  as  are  here  present  are  rare.2 

Still  other  specimens  show,  in  a marked  degree,  the  effects  of  dy- 
namic metamorphism  upon  the  Horse  Bace  rocks.  No,  11189,  from  the 
head  of  the  rapid,  on  the  Michigan  side,  has  a pronounced  gneissic 
structure.  Its  hornblende  is  of  the  usual  character,  sometimes  in  com- 
pact crystalloids  of  large  size,  sometimes  in  a fibrous  aggregate,  but 
almost  always  much  twisted,  bent,  or  broken.  The  feldspar,  in  some 
instances,  is  completely  changed  to  an  aggregate  of  epidote  crystals,  as 
in  the  rock  last  described  ; in  others,  it  merely  has  minute,  highly  re- 
fracting epidote  grains  more  or  less  abundantly  developed  in  it  (saus- 
snritization).  These  are  often  accompanied  by  rhombic  dodecahedra 
of  a colorless  garnet.3  Other  of  the  feldspar  individuals  show  a me- 
chanical rather  than  a chemical  alteration.  There  is,  in  some  cases,  a 

1 A not  unusual  alteration  according  to  Rotli ; Allgemeine  nnd  chemisclie  Geologie,  vol.  1,  1879,  p.  32l. 

2Cohen  mentions  such  a perfect  transformation  of  feldspar  to  epidote  in  the  diorite  which  forms  the 
base  of  the  island  Palma.  Neues  Jahrbuch  fiir  Mineral.,  1876,  p.  751.  Rosenbuseh  also  mentions  them 
in  diorites  from  the  Vosges  Mountains.  Mikros.  Physiog.,  2d  ed.,  vol.  2,  p.  103. 

3 Rosenbuseh:  Mikros.  Physiog.,  2d  ed.,  vol.  2,  p.  136.  Paul  Michael  finds  one  of  the  two  varie- 
ties of  saussurite  in  the  gabbro  of  Wojaleite,  Fichtelgebirge,  composed  of  a lime-alumina  garnet  and 
serpentine.  Neues  Jahrbuch  fiir  Mineral.,  1888,  vol.  1,  p.  39. 


williams.  1 THE  DIORITES  OF  THE  “ HORSE  RACE. 77  109 

peripheral  granulation  (ranclliche  kataklase)  producing  the  “ mortar 
structure77  (Mdrtel-Structur  of  Tornebohm).  In  other  cases  there  is  a 
complete  reduction  of  the  whole  feldspar  crystal  to  a granular  mosaic, 
while  in  still  others  there  is  only  a separation  into  large,  interlocking, 
and  but  slightly  disturbed  areas.  Fine  veins  of  epidote  not  infrequently 
traverse  these  feldspar  crystals.  A jioint  of  mineralogical  importance 
connected  with  this  rock  is  the  evidence  it  affords  of  the  alteration  of 
ilmenite  into  sphene.  The  usual  alteration  product  of  this  mineral, 
leucoxene,  is  now  generally  believed  to  belong  to  this  species,  but  it  is 
rare  to  find  the  crystalline  form  of  the  sphene  so  typically  developed  as 
in  this  section.  The  mineral  is  of  a grayish  brown  color  and  nearly 
opaque,  like  the  secondary  leucoxene  which  surrounds  ilmenite.  It 
polarizes  with  dull  colors,  but  there  is  no  mistaking  its  nature  on  ac- 
count of  its  characteristic  form.  (PI.  XIII,  fig.  I.)1 

No.  11078,  collected  on  the  Wisconsin  side  of  the  river,  just  below 
the  Horse  Eace,  is  perfectly  continuous  with  No.  11077,  above  described, 
and  represents  a phase  of  this  rock  produced  by  the  action  of  intense 
pressure.  The  hornblende  is  almost  wholly  changed  to  an  aggregate 
of  weakly  polarizing  fibers,  which,  according  to  the  descriptions  of 
Eosenbusch,  are  perhaps  best  regarded  as  of  a serpentinous  nature. 
These  twine  in  and  around  the  feldspar  so  as  to  produce  a sort  of 
“ Flaser 77  structure.  The  feldspars  themselves  are  sometimes  reduced  to 
a mosaic ; but  sometimes  they  have  only  a peripheral  granulation.  Much 
of  the  biotite  of  the  unaltered  rock  remains  among  the  alteration  prod- 
ucts of  the  hornblende.  The  iron  ore  has  been  drawn  out  into  sinuous 
stringers  which  follow  the  direction  of  the  foliation. 

No.  11191  was  taken  from  a wavy  schistose,  chloritic  band  on  the 
Michigan  side  of  the  Horse  Eace.  It  has  a strike  30°  E.  of  N.,  and 
traverses  a coarse  grained  massive  greenstone,  into  which  it  passes  by 
insensible  gradations.  In  this  rock  there  is  considerable  hornblende, 
which  is  seen  in  the  process  of  transformation  to  a fibrous,  yellow  ser- 
pentine. The  feldspar  is  of  the  reddish  brown  variety  and  has  under- 
gone granulation  around  the  edge.  This  has  been  accompanied  by  the 
production  of  quartz  and  calcite.  In  a large  area  of  the  latter  mineral 
there  are  crystals  of  a substance  whose  exact  nature  could  not  be  de- 
termined, It  has  the  bluish  interference  colors  of  zoisite,  a parallel 
extinction  and  a biaxial  interference  figure.  It  is  also  changing  to  the 
same  yellow  serpentine  as  the  hornblende.  The  sepentiue  penetrates 
and  traverses  it  as  it  does  crystals  of  olivine.  Chlorite  is  also  a frequent 
component  of  this  rock. 

Nos.  11080  and  11195  are  exceptionally  fine  grained  greenstones,  the 
former  from  the  foot  and  the  latter  from  the  head  of  the  Horse  Eace. 
Both  are  composed  essentially  of  actinolite,  feldspar,  quartz,  and  epi- 
dote, and  resemble  in  their  microscopical  appearance  and  structure  the 

1 Schonck  observed  tho  titanic  iron  entirely  replaced  by  sphene  in  a schistose  diabase  from  the 
upper  Buhr  Valley.  Inaugural  Dissertation,  Bonn,  1884,  p.  57. 


110 


GREENSTONE  SCHIST  AREAS  OF  MICHIGAN. 


[BULL.  62. 


typical  so-called  “ crystalline  schists.”  Still  the  former  is  massive  and 
cuts  across  the  strike  of  schistose  rocks  like  a dike,  while  the  latter  is 
decidedly  schistose.  No.  11195  contains  minute  and  sharp,  dark  brown 
sphene  crystals,  which  appear  to  have  originated,  like  those  in  No. 
11?  89,  from  the  alteration  of  ilmenite. 

THE  ACID  ROCKS  OF  UPPER  QUINNESEC  FALLS  AND  THE  HORSE  RACE. 

Among  the  rocks  to  be  found  in  the  neighborhood  of  the  Upper  Quin- 
nesec  Falls  and  Horse  Race  are  those  of  an  acid  type.  They  occur  in 
bands  of  varying  width,  which  generally,  but  not  always,  conform  to 
the  foliation  of  the  greenstones.  These  acid  rocks  are  sometimes  mass- 
ive granites  without  a trace  of  schistose  structure ; sometimes  gneisses 
with  a “Flaser”  or  “Augen”  structure,  and  sometimes  finely  banded  and 
schistose  rocks  like  the  Saxon  granulites.  Whenever  these  bands  show 
any  indications  of  schistose  structure  this  seems  to  be  conformable  to 
the  cleavage  of  the  adjoining  greenstones,  without  reference  to  what 
the  direction  of  the  band  itself  may  be.  Inasmuch,  however,  as  these 
two  directions  generally  coincide,  it  is  not  common  that  the  foliation  of 
the  acid  bands  makes  any  angle  with  their  sides.  Such  instances  were 
nevertheless  occasionally  found,  and  they  have  a very  important  bear- 
ing on  the  genesis  of  these  rocks  and  on  their  relation  to  the  green- 
stones which  surround  them. 

An  inspection  of  the  published  geological  maps  of  the  region  south 
of  Lake  Superior 1 will  show  that  immediately  south  of  the  portion  of 
the  Menominee  River  under  discussion  there  is  an  enormous  area  of  a 
typical  granite.  Major  Brooks,  in  his  report  on  the  Menominee  dis- 
trict, thinks  that  this  granite  may  very  possibly  be  of  eruptive  origin, 
but,  whether  so  or  not,  that  it  certainly  overlies  and  penetrates  (“in 
veins”)  the  upper  members  of  the  greenstone  series.2  Since,  however, 
he  regards  the  greenstones  as  occupying  the  upper  portion  of  the  Hu- 
ronian  formation,  he  is  compelled  to  assume  that  the  granite  represents 
its  youngest  member  and  hence  he  designates  it  as  the  “Huronian 
granite.”  (See  profile,  Fig.  2.) 

Without  entering  in  this  place  into  a discussion  of  the  stratigraphical 
relationships  of  these  rocks,  it  may  at  least  be  stated  with  certainty 
that  this  granite  does  penetrate  the  greenstones  in  the  form  of  dikes 
and  apophyses,  especially  where  the  main  mass  approaches  nearest  to 
the  river.  This  point  is  about  half  a mile  south  of  the  Horse  Race,  as 
may  be  seen  by  Major  Brooks’s  section  and  map  of  this  region 3.  Here 
the  typical,  coarse  grained  and  somewhat  porphyritic  granite  appears 
in  a high  ridge. 

The  adjacent  greenstones  and  greenstone  schists  do  not  here  materi- 
ally differ  from  those  at  Upper  Quinnesec  Falls.  They  strike  nearly  east 

1 Geol.  Wisconsin,  vol.  3,  atlas,  FI.  XXVIII;  Mon.  U.  S.  Geol.  Survey,  vol.  5,  PI.  I ; Fifth  Ann. 

Kept.  U.  S.  Geol.  Survoy,  FI.  XXII. 

2 Geol.  Wisconsin,  vol.  3,  pp.  452,  531,  719.  3Ibid.,  PI.  Ill,  p.  472. 


WILLIAMS.  1 GRANITE  SOUTH  OF  THE  u HORSE  RACE.  ” 111 

and  west  and  dip  to  the  south.  Near  the  granite  contact  they  are  filled 
with  dikes  of  all  sizes,  evidently  offshoots  from  the  main  granite  mass 
(Nos.  11105  to  11107).  These  dikes,  when  small,  are  fine  grained  and 
felsitic,  but  when  larger  their  texture  is  coarser  and  they  have  fre- 
quently a well  developed  schistose  structure  parallel  to  that  of  the  ad- 
joining schists.  After  a careful  examination  of  this  locality  and  of  the 
exposures  between  it  and  the  river,  there  is  no  .doubt  in  the  writer’s 
mind  that  the  granite,  u Augengneiss,”  biotitic  gneiss,  and  schistose 
porphyry  (or  u por phyroid,”  as  Credner  calls  this  rock)  visible  near  the 
Upper  Quinnesec  Falls  and  along  the  Horse  Bace,  are  also  dikes  or 
aphophyses  connected  with  the  main  southern  granite  area.  The  schis- 
tose or  banded  structure  of  these  rocks,  when  such  exists,  is  a secondary 
feature,  produced  by  the  same  dynamic  agencies  which  rendered  the 
greenstones  themselves  schistose. 

An  intelligent  study  of  these  acid  rocks  should  begin  with  an  exami- 
nation of  the  massive  granite  from  the  large  area  south  of  the  Menominee. 
No.  11104  was  collected  near  the  contact,  about  half  a mile  south  of  the 
Horse  Bace,  where,  after  appearing  in  numerous  dikes  in  the  green- 
stone, the  solid  mass  of  granite  appears  in  an  abrupt  wall,  trending  N. 
80°  E.  This  rock  appears  in  a hand-specimen  to  be  a typical,  coarse 
grained  granitite,  with  a decided  tendency  to  a porphyritic  structure. 
The  latter  feature  may,  however,  be  due  to  the  nearness  of  this  locality 
to  the  contact.  When  examined  under  the  microscope,  the  macroscopic 
diagnosis  is  found  to  be  correct  and  several  additional  points  of  interest 
are  brought  to  light.  The  oldest  constituents  are  zircon  and  apatite; 
both  quite  abundant  in  the  form  usual  in  granitic  rocks.  Iron  oxide 
seems  to  be  almost  absent  as  an  original  constituent,  though  it  is  found 
in  some  of  the  altered  micas.  The  biotite,  the  only  mica  present,  is  not 
abundant.  It  is  invariably  bleached  to  a green  color  by  the  reduction 
of  its  iron  to  the  ferrous  state.  It  contains  abundant  inclusions  of  apa- 
tite, zircon  (around  which  are  pleochroic  aureoles),  and  some  secondary 
magnetite.  No  trace  of  either  hornblende  or  pyroxene  was  observed. 
Sphene,  however,  is  present,  as  are  also  a few  sharp  crystals  of  a dark 
grayish  blue  tourmaline.  The  principal  interest  of  this  rock  attaches  to 
its  feldspar  and  quartz.  They  together  make  up  nearly  the  whole  mass 
and  exhibit,  in  a remarkable  degree,  the  effects  of  pressure.  The  feldspar 
is  of  three  kinds : normal  plagioclase  (oligoclase),  unstriated  orthoclase, 
and  inicrocline.  The  relationship  of  these  species  of  feldspar  is  a sug- 
gestive one.  Both  the  oligoclase  and  the  orthoclase  are  always  altered 
to  a fine  micaceous  or  kaolinitic  product  which  is  particularly  abundant 
in  the  center  of  the  crystals,  a zone  of  the  unaltered  mineral  being  often 
preserved  around  the  edge.  The  microcline,  on  the  other  hand,  almost 
never  shows  any  indication  of  alteration. 

It  is  always  clear  and  fresh  in  appearance,  but  its  twinning  lamellae 
are  bent  or  curved  and  bear  every  sign  of  having  been  secondarily  de- 
veloped.1 In  other  words,  we  have  here  again,  in  the  writer’s  opinion, 

•Rosenbnsc.h,  Mikros.  Phyaiog.,  2d  ed.,  vol.  2,  p.  295. 


112 


GREENSTONE  SCHIST  AREAS  OE  MICHIGAN. 


[BULL.  62. 


a striking  example  of  the  mechanical  action  apparent  in  the  feldspar,  be- 
ing inversely  proportional  to  the  chemical  action  which  has  gone  on  in  it. 
Original  orthoclase  has  been  converted  partly  into  kaolin,  partly  into 
microeline,  according  to  the  way  in  which  the  action  of  the  force  mani- 
fested itself.  The  effect  of  the  force  which  acted  upon  this  rock  is  also 
apparent  in  other  ways.  The  large  original  feldspar  crystals  show  a 
peripheral  granulation  (see  Chapter  I,  p.  49),  and  where  they  have  been 
fissured  their  cracks  are  filled  with  a new  crystallization  of  plagioclase, 
orthoclase,  and  quartz.  None  of  these  minerals  shows  any  signs  of 
chemical  alteration  and  microeline  is  never  to  be  found  among  them. 
Thus  is  produced  a good  example  of  what  Tornebohm  has  called  a mor- 
tar structure  (“Mortel-Structur”)1.  In  this  secondary  cement-like  ag- 
gregate, a micropegmatitic  intergrowth  of  quartz  and  feldspar  is  quite 
common,  and  calcite,  in  good-sized  Individuals,  is  by  no  means  rare. 

The  original  quartz  of  this  granite  also  shows  many  indications  of 
having  been  squeezed.  The  crystals  or  grains  often  have  an  undulatory 
extinction,  Avhile  larger  grains  are  broken  and  the  fragments  are  more 
or  less  displaced.  Proof  that  these  were  not  originally  different  grains  is 
given  in  section  No.  11104,  where  a small  tourmaline  crystal  is  broken 

(See  Fig.  13).  No.  11105  is  a speci- 
men of  the  prevailing  rock  near  the 
granite  contact.  This  is  a horn  blende 
schist,  composed  mainly  of  irregular 
grains  of  dark  green  hornblende  and 
quartz.  There  are  beside  some  stri- 
ated and  some  unstriated  feldspars, 
a little  sphene  and  an  abundance  of 
extremely  sharp  and  clear  epidote 
crystals.  The  banding  of  this  rock 
is  caused  by  the  preponderance  of 
hornblende  in  some  layers  and  of 
quartz  in  others.  Its  strike  is  nearly 
east  and  west  and  its  dip  75°  to 
80°  to  the  south.  Under  the  micro- 
scope all  of  the  constituents  by 
their  extreme  freshness  and  freedom 
from  all  inclusions  convey  the  impression  of  being  secondary  crystal- 
lizations. The  texture  of  the  rock  is  granular,  although  the  epidote 
is  present  either  in  exceedingly  sharp  crystals  (which  often  pass 
unbroken  from  one  quartz  grain  into  another)  or  in  much  more 
minute,  ovoid  granules,  forming  the  little,  highly  refracting  particles 
which  are  so  common  in  the  crystalline  schists.  No.  11107  was 
taken  from  one  of  the  wider  of  the  numerous  acid  dikes  which  pene- 

1N&,gra  oid  om  granit  ocli  gneis.  Geol.  Foren.  Stockholm  Forhandl.,  1880-’81,  vol.  5,  p.  233,  (ref. 
Neues  Jahrbuch  fur  Mineral.,  1881,  vol.  2,  Referate,  p.  51;  and  Roseubuscb,  Mikros.  Pkysiog.,  2d  ed., 
vol.  2,  p.  42.) 

2 Compare  Dr.  Chelius’s  remarks  on  the  Hessian  granite-porphyries,  Notizblatt  des  Vereius  fur  Erd- 
kunde  zu  Darmstadt,  1883. 


and  faulted  just  at  the  contact.2 


Fig.  13.— Broken  tourmaline  crystal  proving 
the  secondary  fracture  of  the  inclosing  quartz 
grain,  “Horse  Race”  granite.  No.  11104. 


WILLIAMS.] 


GRANITE  GNEISSES  OF  THE  “ HORSE  RACE.” 


113 


trate  the  last  described  hornblende  schist  in  the  neighborhood  of  the 
granite  contact.  It  has  a decidedly  gneissic  structure  parallel  to  the 
banding  of  the  inclosing  schist,  which  is  here  also  the  direction  of  this 
band  or  dike.  The  microscope  shows  that  the  mineral  composition  of 
this  rock  is  identical  with  that  of  the  coarse  granite  (No.  11104). 
There  is  the  same  zircon,  sphene,  and  tourmaline  associated  with  the 
biotite,  feldspar,  and  quartz.  The  differences  are  the  gneissic  structure, 
fineness  of  grain  and  absence  of  all  porphyritic  structure  in  the  dike 
rock,  while  none  of  its  constituent  minerals  show  the  chemical  altera- 
tion which  has  progressed  so  far  in  the  massive  granite.  Both  the 
biotite  and  the  feldspar  are  quite  fresh,  the  rich  brown  color  of  the  for- 
mer contrasting  with  green  and  bleached  mica  above  described. 

After  the  foregoing  review  of  the  character  of  the  acid  rocks  at  and 
near  the  granite  contact,  we  are  in  a much  better  condition  to  under- 
stand the  occurrence  of  the  bands  of  gneiss  and  porphyroid  near  the 
Upper  Quinnesec  Falls,  which  were  observed  by  Major  Brooks  and  Prof. 
Pumpelly.1  If  we  now  examine  some  of  the  most  typical  of  these  ex- 
posures with  care,  we  shall  find  that  they  are  quite  identical  with  the 
rocks  which  we  have  just  been  considering. 

On  the  lower  side  of  a small  cove  which  indents  the  Wisconsin 
river  bank  immediately  below  the  Horse  Race  there  is  a narrow  band 
of  acid  rock  well  exposed  on  the  shore.  The  center  of  this  band  is  com- 
posed of  a massive,  gray  colored,  porphyritic  rock  resembling  a granite 
(No.  11082).  This  grades  on  both  sides  imperceptibly  into  a well  char- 
acterized, fine  grained  gneiss  (No.  11085),  which  in  places  is  so  finely 
banded  as  to  resemble  some  of  the  Saxon  granulites  (No.  11084).  The 
foliation  of  this  exposure  is  nearly  vertical  and  seems  to  be  quite  par- 
allel to  the  sides  of  the  band,  which  itself  makes  only  a slight  angle  with 
the  cleavage  of  the  adjoining  greenstones. 

No.  11082  was  collected  from  the  central  and  most  massive  portion 
of  this  acid  band.  Macroscopically  the  rock  appears  to  be  a typical 
granite  porphyry,  nor  does  the  examination  of  a thin  section  with  the 
microscope  reveal  anything  opposed  to  this  determination.  The  follow- 
ing analysis  of  the.  rock,  however,  made  by  Mr.  R.  B.  Riggs,  shows  that 
this  rock  is  in  reality  a diorite  : 


Silica  (Si02) 

Alumina  (A120;5) 

Ferric  oxide  (Fe20;j)  . 
Ferrous  oxide  (FeO)  . 

Lime  (CaO) 

Magnesia  (MgO) 

Soda  (Na20) 

Potash  (KjO) 

Water  (H20) 

Carbou  dioxide  (CO.) 


54.83 
25.  49 
1.61 
1. 65 
6.  08 
1.96 
5.  69 
1.87 
1.18 
.18 


Total 


100.  54 


Bull.  02 8 


Gool.  Wisconsin,  vol.  3,  p.  474, 


114 


GREENSTONE  SCHIST  AREAS  OF  MICHIGAN. 


[bull.  62. 


The  microscope  discloses  good-sized  crystals  of  a striated  and  zonally 
formed  feldspar  embedded  in  a granular  mosaic  of  clear,  colorless,  and 
unstriated  grains  associated  with  brown  leaflet  of  biotite.  Apatite, 
zircon,  and  a reddish  pleochroic  sphene  are  also  present  in  small  crys- 
tals. . In  spite  of  this  rock  showing  no  indication  whatever  of  altera- 
tion, it  contains  calcite  in  considerable  quantity.  This  mineral  appar- 
ently penetrates  and  includes  all  the  other  constituents  in  a manner 
which  has  led  Hawes,1  Tornebohm,2  and  Chrustsclioff,3  to  regard  it 
under  similar  circumstances  as  a product  of  the  original  crystallization. 

In  one  section  of  the  present  rock  sharply  defined  sphene  crystals  were 
observed  wholly  surrounded  by  the  calcite.  Nevertheless  the  presence 
of  this  carbonate  in  the  fresh  rock  is  to  be  explained,  as  Rosenbusch 
suggests,  by  the  filling  up  of  drusy  or  miarolitic  cavities.4 

The  rock  appears  both  raacroscopically  and  microscopically  to  be  a 
granite  porphyry  with  a microgranitic  groundmass.  The  analysis,  how- 
ever, shows  it  to  be  largely  composed  of  a feldspar  of  the  andesine 
series,  and  this  is  also  indicated  by  a further  examination.  The  color- 
less grains  of  the  groundmass,  in  spite  of  their  limpid  character  and 
superficial  resemblance  to  quartz,  give  in  converged  polarized  light  the 
brush  or  hyperbola  of  a biaxial  crystal.  In  the  Thoulet  solution  the 
colorless  portion  6f  the  powder  fell  between  2.683  and  2.650,  a large 
proportion,  however,  being  confined  between  the  limits  2.668  and  2.659. 

A small  proportion  possessed  exactly  the  specific  gravity  of  quartz, 
so  that  it  is  impossible  to  say  with  certainty  whether  this  mineral  is 
present  in  the  groundmass.  The  relative  proportions  of  silica  and 
alumina,  however,  as  given  by  the  analysis,  make  this  improbable.  We 
must  describe  this  rock  as  a very  pure  type  of  a mica-diorite  porphyry  ; 
whose  groundmass  is  composed  of  a mosaic  of  clear  unstriated  lime- 
soda  feldspar,  probably  andesine. 

The  two  specimens  (Nos.  11084  and  11085),  taken  from  the  gneissic 
portion  of  this  exposure,  when  seen  under  the  microscope,  closely  re- 
semble the  groundmass  of  the  diorite  porphyry  just  described.  The 
chief  difference  is  in  the  banded  appearance,  produced  by  the  parallel 
arrangement  of  the  grains,  and  especially  of  the  mica  x>lates.  This  is 
most  pronounced  in  No.  11084,  where  the  mica  is  collected  in  certain 
layers  and  where  there  is  also  an  alternation  in  the  grain,  some  layers 
being  coarser  and  others  finer.  Occasional  tourmaline  crystals  are 
here  associated  with  the  zircon  and  apatite.  Calcite  also  is  present,  as 
in  the  last  described  rock,  but  now  it  is  in  stringers  and  arranged,  like 
all  the  other  components,  in  the  direction  of  the  schistosity.  No.  11085 
has  neither  the  calcite  nor  the  tourmaline.  Its  most  interesting  feature 
is  the  presence  of  long  strings  of  minute  rutile  crystals  which  appear  to 

1 Geology  ot  New  Hampshire,  vol.  3,  Part  IV : Mineralogy  and  Lithology,  1878,  p.  208,  PI.  XII,  Fig.  1..  { 

20m  Kalkgranit.  Geol.  Fdceu  Stockholm  Forhandh,  vol.  3,  1876,  p.  210.  Om  Kalcithalti  graniter. 
Kong.  Vetensk.  ak.  Fdrhandl.,  vol.  5,  1881,  p.  233. 

3 Bull.  Soe.  Mineral,  de  France,  vol.  8,  1885,  p.  137. 

4Mikros.  Physiog.,  2d  ed.,  vol.  2,  1885,  p.  34. 


WILLIAMS.] 


GRANITE  GNEISSES  OF  THE  u HORSE  RACE.”  115 

have  originated  from  the  alteration  of  the  biotite.  No.  11079,  collected 
from  a narrow  acid  band  slightly  east  of  this  exposure,  is  quite  ident- 
ical in  both  composition  and  structure  with  the  two  last  mentioned 
rocks.  There  are  here  occasional  re- 
mains of  former  porphyritic  feldspar 
crystals  which  have  been  mostly  de- 
stroyed by  granulation.  Tourmaline 
is  quite  abundant,  as  are  also  flakes  of 
colorless  but  brightly  polarizing  sericite. 

It  will  be  seen  that  these  rocks  are 
quite  the  same  as  those  found  farther 
south  at  the  granite  contact.  Along 
the  whole  extent  of  the  Horse  Race 
similar  acid  rocks  are  very  abundant. 

They  occur  in  bands  varying  from  the 
finest  seams  to  such  as  are  many  yards 
in  width.  While  these  as  a rule  follow 
the  direction  of  the  foliation  of  the 
greenstones,  they  by  no  means  always 
do  so.  Their  mode  of  occurrence  often 
bears  strong  testimony  to  their  intru- 
sive nature,  as  may  be  seen  from  the 
following  figures  sketched  at  the  head 
of  the  Horse  Race  on  the  Michigan  side 
of  the  river. 

Fig.  14  shows  two  bands  of  gneiss,  one  parallel  to  the  strike  of  the 
greenstones,  the  other  cutting  across  it.  Iu  each  the  lamination  of  the 
acid  rock  coincides  with  that  of  the  greenstones,  without  regard  to  the 
sides  of  the  band.  This  would  seem  conclusive  evidence  of  the  second- 
ary nature  of  the  gneissic  structure. 


cove  at  tlic  head  of  the  Horse  Race.  Direc- 
tion of  the  shading  lines  indicates  the 
strike. 


Fig.  15. — Foliated  granite  (gneiss)  intrusive  in  greenstone.  Head  of  the  Horse  Race. 

Fig.  15  shows  a band  of  gneiss  which  comes  to  an  abrupt  termina- 
tion in  the  greenstone  and  which  sends  out  apophyses  into  this,  as  only 
an  intrusive  dike  would  do. 


116 


GREENSTONE  SCHIST  AREAS  OF  MICHIGAN, 


[BULL.  62. 


Fig.  16  shows  an  irregular  area  of  gneiss  penetrating  the  greenstone. 
The  lines  in  the  drawing  indicate  the  direction  of  the  foliation.  This 
may  be  a cross-section  of  a laterally  intrusive  arm. 


Fig.  16.— Foliated  granite  (gneiss)  intrusive  in  greenstone.  Head  of  the  Horse  Race. 

Many  other  exposures  might  be  selected  to  prove  the  intrusive 
nature  of  these  acid  rocks  at  the  Upper  Quinnesec  Falls,  but  the  oues 
already  cited  will  suffice  for  the  present  purpose. 

With  respect  to  their  structure,  the  acid  rocks  of  the  Upper  Quin- 
nesec Falls  and  Horse  Race  may  be  classified  as  follows : 

I.  Porphyntic: 

Granite  porphyry,  represented  by  Nos.  11104,  11082,  11087, 
11089,  11190. 

Augen-Gneiss,  represented  by  Nos.  11184,  11193  11196. 

Schistose  porphyry,  represented  by  Nos.  11050,  11051,  11052, 
11096. 

II.  Non-porphyritic : 

Gneiss,  represented  by  Nos.  11079,  11084,  11085,  11188. 

Felsite,  represented  by  No,  11071. 

The  main  points  of  interest  will  now  be  stated  with  reference  to  each 
of  these  types  in  succession,  although  no  further  mention  will  be  made 
of  those  specimens  which  have  already  been  described,  viz,  Nos.  11104, 
11082,  11084,  11085,  11079. 

It  is  believed  that  the  distinctive  features  of  the  schistose  and 
banded  rocks  of  this  region  have  to  a great  extent  been  produced  by 
secondary  causes.  An  original  porpliyritic  structure  seems  to  have  been 
very  prevalent,  if  not  universal,  in  all  of  these  acid  dikes.  We  are  able 
to  trace  its  gradual  disappearance,  and  we  find  that  this  is  proportional 
to  the  intensity  of  the  dynamic  action  to  which  the  particular  rock  has 
been  subjected.  The  crushing  or  rubbing  of  the  constituent  minerals 
against  one  another  has  produced  a peripheral  granulation  (u  randliclie 
Kataklase”).  This  has  altered  the  porpliyritic  crystals  into  the  eyes 
or  “Augen”  of  the'  gneisses  and  schistose  porphyries,  as  is  shown  in 
PI.  XV,  fig.  1 ; and  there  seems  no  reason  why  its  extreme  applica- 
tion may  not  have  changed  a porpliyritic  rock  to  a felsite. 


WILLIAMS.] 


ORTHITE  IN  GRANITE. 


117 


Granite  porphyry. — No.  11190,  from  the  Michigan  side  of  the  Horse 
Race,  near  its  center,  is  from  a small  area  of  acid  rock  exposed  at  the 
water’s  edge,  which  seems  to  be  completely  surrounded  on  the  three 
other  sides  by  diorite.  It  is  porphyritic,  bat  contains  a very  large  pro- 
portion of  feldspars  (mostly  striated)  and  comparatively  little  ground - 
mass.  This  latter  is  so  arranged  as  to  produce  a resemblance  to  the 
mortar -structure,  and  thus  the  rock  approaches  No.  11101,  although  all 
of  its  quartz  is  confined  to  the  groundmass.  Biotite  is  quite  abundant. 
It  contains  fine  pleochroic  aureoles,  and  is  frequently  bleached  to  a 
pale  green  color. 

Nos.  11087  and  11089,  both  from  the  Wisconsin  bank  of  the  Horse 
Race,  are  decidedly  porphyritic.  A fine  grained  granular  groundmass 
is  in  sharp  contrast  to  the  well  formed  feldspar  crystals.  These  are 
noticeable  on  account  of  their  finely  developed  zonal  structure,  which 
is  produced  sometimes  by  a concentric  arrangement  of  inclusions,  some- 
times by  a variation  of  composition  and  extinction  angles  in  different 
layers.  The  zonal  structure  of  the  feldspars  in  these  rocks  is  as  per- 
fect as  it  is  in  the  more  modern  andesites.  The  mica  in  No.  11087  is 
biotite  of  the  usual  character,  but  in  No.  11089  muscovite  is  equally 
abundant,  making  this  latter  rock  a ^rue  granite  instead  of  a granitite. 
Some  of  this  muscovite,  at  least,  may  be  plainly  seen  to  have  originated 
from  the  alteration  of  the  orthoclase.  In  many  cases  it  lies  in  brilliantly 
polarizing  flakes  of  considerable  size,  clustered  together  in  the  center 
of  the  orthoclase  crystals,  which  portion  always  appears  to  be  the  most 
subject  to  alteration. 

These  rocks  show  to  a moderate  degree  the  effects  of  pressure  which 
are  most  manifest  in  the  porphyritic  quartzes.  These  are  much  dis- 
torted and  often  broken  and  granulated,  as  shown  in  PI.  XV,  fig.  2. 
It  seems  at  first  thought  strange  that 
the  harder  quartz  should  be  more  sus- 
ceptible to  pressure  than  the  softer 
feldspar,  and  yet  this  is  known  to  be 
a well  established  fact,  as  has  been 
observed  in  Chapter  I.  The  brittle- 
ness of  the  quartz  causes  it  to  break, 
where  the  feldspar  is  only  bent  or 
distorted,  without  rupture. 

In  some  cases  the  feldspar,  as  well  as 
the  quartz,  6hows  a slight  peripheral 
granulation  and  passage  into  a mosaic, 
which  can  not  be  distinguished  from 
the  groundmass.  This  is  in  all  in- 
stances, however,  only  incipient,  while 
the  main  portion  of  the  groundmass  is  an  original  feature  of  the  rock. 

In  the  granitites,  Nos.  11087  and  11190  an  unusual  constituent  is 
present.  This  is  in  sharp  crystals  of  good  size  (2  by  3""")  and  has  the 
shape  of  epidote.  Its  color  is  yellowish  brown  or  greenish  yellow. 


Fig.  17. — Orthite  in  granite.  Horae  Race 
Rapid.  No.  11087.  Magnified  80  diameters. 


118 


GREENSTONE  SCHIST  AREAS  OF  MICHIGAN. 


[bull.  62. 


it  seems  to  have  undergone  partial  alteration,  and  agrees  closely  with 
the  published  descriptions  of  orthite  (allanite).1  The  two  crystals  in 
section  No.  11087,  although  by  no  means  entirely  changed,  appear  to 
be  completely  isotropic,  a peculiarity  especially  mentioned  by  Rosen- 
busch  as  not  uncommon  to  orthite.2 

Augen-Gneiss. — The  best  example  of  this  type  is  No.  11184,  from  the 
Michigan  side  of  the  Horse  Race.  With  reference  to  this  rock  the  fol- 
lowing is  extracted  from  the  field  notes  made  in  July,  1885: 

A short  distance  above  the  mouth  of  the  Horse  Race  the  ridge  is  cut  by  a ravine. 
Here,  near  the  water’s  edge,  are  some  beautifully  porphyritic,  red,  acid  rocks,  occur- 
ring apparently  as  dikes  in  the  greenstone.  The  direction  of  these  dikes  is  quite 
irregular.  Their  width  also  varies  continually.  They  contain  a deep  red  feldspar,  a 
white  feldspar,  and  quartz  in  porphyritic  crystals.  When  much  of  the  first  mentioned 
feldspar  is  present,  the  rock  is  very  red  ; when  it  is  absent  it  is  gray.  Both  varieties 
may  occur  in  the  same  specimen.  These  rocks  show  the  effects  of  pressure  very  finely.  i 
The  porphyritic  crystals  form  “ Augen,”  around  which  the  groundmass  bends.  The 
direction  of  the  banding  when  well  marked  appears  to  be  parall  1 to  the  walls  of  the 
dikes.  The  “ Augen”  stand  vertically. 

Under  the  microscope  the  banded  or  gneissic  structure  of  this  rock  is 
as  well  marked  by  the  lenticular  (“  Flaser ”)  arrangement  of  the  mica  as  in 
the  hand-specimen.  Its  most  instructive  feature  is  the  formation  of  the 
eyes  (“Augen.”)  and  the  gradual  disappearance  of  the  large  porphy- 
ritic feldspar  crystals  by  peripheral  granulation  due  to  pressure.  A ] 
typical  example  of  this  is  represented  in  PI.  XV,  fig.  1.  Here  it 
will  be  seen  that  a large  porphyritic  crystal  of  triclinic  feldspar  has  been 
granulated  on  two  opposite  sides,  corresponding  to  the  direction  of  the 
schistosity,  and  that  the  material  thus  formed  has  been  drawn  out  into 
a lenticular- shaped  mass,  with  the  remaining  solid  portion  of  the  feld- 
spar as  its  center.  This  forms  the  eye  or  “ Auge”  around  which  the 
groundmass  is  seen  to  curve.  Such  a structure  has  been  described  and 
figured  by  J.  Lehmann 3 and  others.  It  is  important  to  observe  that  the 
secondary  granulation  has  here  produced  a mosaic  of  much  coarser  grain 
than  the  surrounding  groundmass.  This  corresponds  to  observations 
of  Dr.  Chelius,  made  on  certain  Hessian  granite  porphyries.4 

No.  11196,  from  the  head  of  the  Horse  Race,  on  the  Michigan  side,  is  5 

described  in  the  field  notes  as  “ a typical  biotite  gneiss  with  a wavy  I 

structure,  the  biotite  lamellae  (secondary?)  winding  around  the  porphy- 
ritic crystals  of  feldspar  and  quartz.”  Under  the  microscope  the  ground- 
mass  is  seen  to  be  fine  grained,  and,  to  some  extent  at  least,  to  have 
originated  from  the  granulation  of  the  porphyritic  crystals,  which  ex- 
hibit this  process  in  an  admirable  manner.  Dark  brown  biotite  and 
sphene  are  common.  Zircon  and  apatite  are  also  present.  The  quartz 

» 

'A.  Sjogren,  Geol.  Fiiren.  Stockholm  Forliandl.,  vol.  3,  1876,  p.  258,  Tbrnebohm  Under  Vega-Expe*  j 
ditionen  insamlade  hergarter.  Vega-Exped.  vetensk.  jakttagelser,  VI,  Stockholm,  1884,  p.  124.  Cross 
& Iddings,  Am.  Jonr.  Sci.,  3d  series,  vol.  30, 1885,  p.  108. 

2 Mikros.  Pbysiog.,  2d  ed.,  vol.  1,  p.  499. 

3 Untersuclmngen  iiber  die  Entstehung  der  altkrystallinischon  Schicfergesteine.  Eonn,  1884. 

4 Notizblatt  des  Vereins  fur  Erdkunde  zu  Darmstadt,  4.  Folge,  5 Heft.,  1885,  quoted  by  Roaenbusch, 
Mikros.  Pbysiog.,  2d  ed.,  vol.  2,  p,  294. 


Williams.]  SCHISTOSE  PORPHYRIES  OF  THE  a HORSE  RACE.”  119 

is  in  large  granular  areas.  Rows  of  fluid  cavities  traverse  the. grains 
and  pass  uninterruptedly  from  one  to  another. 

The  following  analysis  of  this  rock  is  also  by  Mr.  R.  B.  Riggs : 


Silica  (Si02) 67.77 

Alumina  (A1203) 16.61 

Ferric  oxide  (Fe203) 2.06 

Ferrous  oxide  (FeO) 1. 96 

Lime  (CaO)  1.87 

Magnesia  (MgO) 1.26 

Soda.(Na,0) 4.35 

Potash  (K,0) 2.35 

Water  (H,0) 1. 69 

Carbon  dioxide  (C02) 19 


Total 100.11 


This  is  much  more  like  the  analysis  of  a granitite  than  the  last  one 
given  (No.  11082),  but  the  preponderance  of  soda  over  potash  indicates 
the  presence  of  a large  amount  of  soda  orthoclase. 

Schistose  Porphyries  or  Porpliyroids. — Just  below  Upper  Quinnesec 
Falls,  especially  on  the  Wisconsin  side,  are  good  exposures  of  finely 
schistose  acid  rocks.  They  contain  small  porphyritic  crystals  of  feld- 
spar and  quartz,  and  a considerable  amount  of  sericite  or  hydro-mica, 
which  winds  around  these  crystals  so  as  to  produce  a lenticular  or 
“ Flaser  ” structure.  In  color  they  present  every  shade  from  flesh  red 
to  gray. 

Rocks  of  this  general  type  have  a wide  distribution  and  have  arrested 
the  particular  attention  of  petrographical  investigators.  In  some  in- 
stances they  have  been  conclusively  shown  to  be  the  product  of  the 
metamorphism  of  fragmental  rocks — either  tuffs  or  true  sediments — 
while  in  other  cases  they  have  resulted  from  the  action  of  great  dynamic 
forces  upon  massive  rocks  of  a corresponding  composition,  i.  e.  quartz 
porphyries.  When  it  is  possible  to  trace  with  certainty  the  origin  of 
these  rocks  to  stratified  deposits  they  are  usually  designated  asporphy- 
roids , while  in  case  their  mother-rock  can  be  shown  to  have  been  quartz 
porphyry  they  are  usually  called  schistose  porphyries.  In  their  extreme 
development  these  two  types  are  often  petrographically  indistinguish- 
able and  they  present  an  instructive  instance  of  the  production  of  identi- 
cal results  by  the  action  of  the  same  physical  forces  upon  matter  of  the 
same  average  composition,  though  differing  widely  in  origin  and  its 
structure.1 

The  schistose  porphyries  occurring  at  Upper  Quinnesec  Falls  were 
made  the  subject  of  an  extended  paper  by  Hermann  Oreduer,  published 
in  3870.2  This  author  concludes  from  a macroscopical  examination  that 
these  rocks  are  altered  sediments  which  are  interpolated  between  the 


' Hull.  U.  S.  Geol.  Survey,  No.  28,  p.  1. 

2Uober  Nordamerikani«cke  Schioferporpliyroido.  Nencs  Jalirlmch  fiir  Mineral.,  1870.  pp. 970-984. 


120 


GREENSTONE  SCHIST  AREAS  OF  MICHIGAN. 


[bull.  62. 


diabase  beds  of  tbe  Upper  Huronian.  He  divides  their  whole  ex- 
posure at  this  locality,  which  he  gives  as  300  feet,  as  follows: 

Feet. 


(b)  Weakly  schistose  orthoclase  porphyroid 50 

(c)  Typical  feldspar-paragonite  schist 10 

(d)  Light  liesh-red  orthoclase-paragonite  schist 30 

(e)  Paragonite  schist 15 

(f)  Lime-paragonite  schist 15 

(g)  Light  reddish  gray  schistose  porphyroid 30 

(h)  Lime-chlorite  schist 50 

(i)  Chlorite  schist * 100 

Total 300 


Of  (b),  (c),  (d),  and  (e)  he  gives  the  following  analyses : 


(b) 

(c) 

(d) 

(e) 

Si02 

66.  70 

72.45 

76.  505 

75.5 

A1202  

15.  90 

8.85 

7.  950 

8.6 

Fe203 

4.  70 

6.  20 

8. 875 

2.6 

MnO 

tr. 

tr. 

tr. 

CaO 

tr. 

tr. 

0.  322 

7.2 

MgO 

tr. 

1.  2 

K20 

8.  06 

9.  24 

1.025 

0.3 

Na,0 

5. 50 

3. 70 

4.384 

3.0 

H20 

1.  5 

Total 

100. 8G 

100. 44 

90.  061 

99.9 

In  discussing  these  analyses  Oredner  finds  sufficient  proof  that  ortho- 
clase alone  is  present,  from  the  fact  that  the  potash  increases  propor- 
tionately with  the  amount  of  feldspar,  and  in  the  absence  of  a twinning 
striation  which  is  visible  to  the  naked  eye.  The  sodium  he  attributes 
entirely  to  the  mica,  which,  in  consequence,  he  names  paragonite. 
The  proof  of  sedimentary  origin  he  finds  in  the  constant  parallelism  of 
the  schist  planes  with  the  limit  between  these  rocks  and  the  adjoining 
diabase ; and  yet  he  cannot  help  being  much  struck  with  the  alterna- 
tion of  such  widely  diverse  rocks  in  a single  and  comparatively  thin 
complex.1 

My  studies  of  these  rocks,  both  in  the  field  and  in  the  laboratory, 
have  led  me  to  results  quite  the  reverse  of  those  obtained  by  Credner. 
Nos.  11050  to  11053  were  collected  from  the  most  typical  band,  which 
here  stands  nearly  vertical  and  strikes  20°  S.  of  E.  They  are  all  essen- 
tially the  same  in  everything  except  color.  They  contain  more  or  less 
rounded  porphyritic  crystals  of  quartz  and  a red  or  grayish  feldspar, 
imbedded  in  a matrix  apparently  composed  of  a yellowish  gray,  greasy- 
feeling  hydro-mica.  >. 

1 Dio  ebenerwaknte  Wecksellagerung  vollkomtuen  versckiedenartiger  Gesteine  ala  zusammen" 
gekdrige  Glieder  einer  wenig  niacktigen  Sckicktenreilio  ist  lioekst  aufiallig.  Zwiacken  zwei  Lagern 
von  Diabas,  also  einom  narqentlicli  aus  Kalkfeldspath  und  Augit  bestekenden  basiscken  Gesteine  rait 
etwa 54  Proc.  Kieaelsiiuro  tritt  zumickst  eiuo  Zone  von  sauren  quarzreickon  Kali fel d apafck-N at  rongliru  - 
lncr-Porpkyroiden  mit  iiber  70  Proc.  Kieselsaure,  aber  okuo  Kalkgekalt  auf,”  etc.  — Loc.  cit.,  p.  981. 


williams.]  SCHISTOSE  PORPHYRIES  OF  THE  “ HORSE  RACE.”  121 

The  following  analysis  of  No.  11050  by  Mr.  K.  B.  Biggs  shows  its 
essential  identity  with  Credner’s  specimen  (b).  Almost  the  only  dif- 
ference is  the  smaller  amount  of  alkali,  although  the  relative  propor- 
tions remain  about  the  same.  Iu  Credner’s  analysis  the  CaO  and 
MgO,  which  make  up  this  difference,  do  not  appear  to  have  been  deter- 


mined. 

Silica  (SiO,) 6G.  60 

Alumina  (A1203) 16.69 

Ferric  oxide  (Fe203) 2.  06 

Ferrous  oxide  (FeO) 93 

Lime  (CaO) 1.40 

Magnesia  (MgO) 1. 15 

Soda  (Na20)  2.46 

Potash  (K20)  5.23 

Water  (H20) 1.70 

Carbon  dioxide  (002) 1. 42 


Total 99.73 


This  is  evidently  the  analysis  of  an  orthoclase  rock,  and  yet  the  micro- 
scope shows  that  a considerable  proportion  of  the  porphyritic  feld- 
spars are  striated  and  triclinic,  iu  spite  of  the  fact  observed  by  Cred- 
ner,  that  this  character  is  not  apparent  to  the  unaided  eye.  We  may 
therefore  reasonably  suppose  that  the  potash  exists  largely  in  the 
grouudmass  and  in  the  secondary  hydro-mica,  which  is  to  be  regarded 
as  true  sericite,  and  not  paragonite  as  assumed  by  Credner. 

The  microscope  discloses  in  all  the  thin  sections  of  these  rocks  the 
typical  structure  of  a quartz  porphyry  modified,  however,  by  the 
action  of  great  pressure.  An  idea  of  it  may  be  obtained  from  PI. 
XIV,  fig.  1,  which  represents  No.  11050.  The  fine  grained,  micro- 
granitic  grouudmass  is  still  present,  inclosing  the  porphyritic  quartzes 
and  feldspars.  The  former  often  exhibit  their  characteristic  dihexa- 
hedral  form,  but  they  are  broken  and  possess  an  undulatory  extinction. 
The  feldspars  are  most  instructive.  They  possess  a sharply  defined 
crystal  form  which,  however,  has  been  cracked  and  the  fragments  have 
been  more  or  less  separated  in  the  direction  of  the  schistosity,  while 
brightly  polarizing  sericite  scales  have  been  abundantly  developed 
in  all  the  fissures.  Sericite  is  also  abundant  in  the  grouudmass,  where  it 
appears  to  have  been  formed  from  the  orthoclase.  Its  scales  are  par- 
allel throughout  the  rock,  to  which  fact  the  schistose  structure  is  al- 
most wholly  due.  The  original  biotite  of  these  rocks  is  now  entirely 
represented  by  a pale  green  chlorite.  During  the  process  of  this  al- 
teration, iron  has  separated  in  the  form  of  opaque,  black  grains;  and, 
in  some  instances  (11050  and  11052),  colorless  but  very  highly  re- 
tractive grains  have  been  produced.  These  sometimes  possess  a sharp 
octahedral  form  and  are  probably  anatase,  formed  from  the  titanic  acid 
of  the  original  biotite,  as  described  by  Stelzner.1  In  and  around  this 
chlorite,  tourmaline  is  also  abundant  either  in  single  individuals  or  in 
groups  of  crystals.  Zircon  and  apatite  are  sparingly  present.  One 


1 Neuea  Jalirbudi  fur  Mineral.,  1884.,  vol.  1,  p.  273. 


122 


GREENSTONE  SCHIST  AREAS  OF  MICHIGAN. 


[BULL.  62. 


remarkably  large  (.4  x .04mm)  crystal  of  the  former  mineral,  which  has 
been  curiously  broken,  is  represented  in  Fig.  18,  taken  from  No.  11052. 

Calcite  is  not  uncommon  and  is  al- 
ways of  a secondary  nature.  In  Nos. 
11051  and  11053  it  forms  a more  or 
less  complete  border  around  the  por- 
phyritic  crystals. 

As  already  stated,  all  four  speci- 
mens collected  from  this  locality  are 
essentially  identical.  No.  11053  is 
more  finely  schistose,  owing  to  its 
more  advanced  stage  of  alteration 
and  the  consequent  greater  produc- 
tion of  sericite.  In  spite  of  this,  how- 
ever, the.  original  structure  is  still 
plainly  visible.  No.  11096  was  ob- 
tained on  the  Michigan  side  of  the 
river,  at  the  foot  of  the  Horse  Race.  It  has  a very  pronounced  schis- 
tose structure,  and,  under  the  microscope,  appears  nearly  identical 
with  the  rocks  just  described  from  below  the  falls,  but  is  not  so  highly 
altered.  Its  biotite  is  in  its  original  fresh  state,  its  porphyritic  crystals 
are  more  intact,  and  sericite  is  not  so  abundantly  developed. 

Gneiss. — In  addition  to  thenonporphyritic  gneisses  already  described, 
Nos.  11079,  11084,  and  11085  (see  pp.  114-115)  one  other  may  be  men- 
tioned, No.  11188,  from  the  head  of  the  Horse  Race,  on  the  Michigan  side. 
This  is  apparently  a typical  biotite  gneiss,  but  it  is  seen  to  pass  by 
gradual  transitions  into  the  hornblende  gneiss  No.  11189  (see  p.  108). 
The  microscope  shows  that  there  are  many  points  of  resemblance  be- 
tween these  two  rocks.  In  the  present  case,  although  quartz  is  abun- 
dant, ampkibole  and  the  same  sphene  observed  in  No.  11189  are  frequent, 
and  the  feldspar  is  of  such  a nature  as  to  be  sTibject  to  saussuritization. 

Felsite. — True  nonporphyritic  felsite  is  not  common  among  the  acid 
rocks  of  the  area  about  the  Upper  Quinnesec  Fall  and  the  Horse  Race. 
The  most  typical  specimen  of  this  class  is  No.  11071,  which  occurs  in 
narrow  bands  in  the  schistose  greenstones  below  the  falls  on  the  Mich- 
igan side  of  the  river.  This  is  a very  compact,  flesh  colored  rock  re- 
sembling jasper.  Under  the  microscope  it  is  seen  to  be  essentially 
identical  with  the  groundmass  of  the  porphyritic  rocks  above  described; 
and  even  here  stretched  and  distorted  crystals  of  quartz  and  feldspar 
are  not  entirely  wanting,  though  they  are  rare. 

There  is,  therefore,  strong  evidence  in  favor  of  the  view  that  the  acid 
rocks  of  the  Upper  Quinnesec  region  are  of  eruptive  origin  ; that  they 
are  to  be  regarded  as  apophyses  wThich  diverged  from  the  granitic  mass, 
to  the  south;  and  that  their  schistose  structure,  when  present,  is  to  be 
attributed  to  secondary  causes. 


Fig.  18. — Broken  zircon  crystal  in  schistose 
porphyry.  Upper  Quinnesec  Falls.  No.  11052. 
Magnified  180  diameters. 


WILLIAMS.] 


ERUPTIVE  ORIGIN  OF  THE  ACID  ROCKS. 


123 


This  evidence  may  be  summarized  as  follows: 

First.  The  structure  of  these  rocks,  as  revealed  by  the  microscope, 
in  spite  of  its  frequently  being  disguised  by  the  action  of  secondary 
causes,  is  always  that  recognized  as  characteristic  of  massive  or  igneous 

rocks. 

Second.  There  are  present  in  these  gneissoid  bands  granitic  facies 
which  agree  exactly  with  the  rock  of  the  main  granite  area,  and  the 
bands  themselves  are  identical  with  others  near  the  contact,  which  can 
be  plainly  seen  to  be  radiating  apophyses  or  dikes. 

Third.  The  schistosity  of  these  bands  is  often  independent  of  their 
direction  and  agrees  with  the  prevailing  strike  of  the  surrounding 
greenstones. 

Fourth.  There  is  abundant  microscopic  evidence  that  the  constitu- 
ents have  been  fractured,  stretched,  and  crushed  since  their  solidill 
ation. 

The  localities  thus  far  considered  on  the  Menominee  Eiver,  viz : 
Sturgeon,  Lower  and  Upper  Quinnesec  Falls,  contain  all  the  important 
exposures  of  crystalline  rocks,  belonging  to  what  Major  Brooks  has 
regarded  as  the  southern  of  the  two  belts  of  greenstone.  If  his  loca- 
tion of  these  rocks  is  correct,  the  members  of  the  northern  belt  appear 
upon  the  river  at  three  points,  viz:  Four-foot  Falls,  Lower  Twin,  and 
Upper  Twin  Falls,  of  which,  however,  the  two  latter  are  connected  by 
almost  continuous  rock  exposures.  These  localities  we  shall  now  pro- 
ceed to  consider  in  detail. 


FOUR-FOOT  FALLS. 

The  exposures  at  this  place  are  represented,  together  with  those  at 
both  the  Twin  Falls,  upon  Major  Brooks’s  map,  which  is  here  repro- 
duced in  PI.  VI.  The  fall  is  hardly  entitled  to  be  so  called,  as  the 
rocks  have  formed  nothing  more  than  a rapid  in  the  river.  Just  at 
the  foot  of  this  rapid  the  river  is  crossed  by  the  Chicago  and  North- 
western Kailroad  bridge,  immediately  beyond  which  a cutting  has 
disclosed  some  very  instructive  exposures  of  the  greenstones.  The 
rocks  may  be  seen  in  position  on  either  side  of  the  river  for  some  dis- 
tance above  the  bridge.  Brooks  distinguishes  upon  his  map  many 
alternating  beds  of  massive,  schistose,  and  slaty  rocks  ( a to  n in  his 
section).  The  beds  here  strike  about  S 80°  E — nearly  at  right  angles 
to  the  direction  of  the  river  at  this  point— and  yet  are  mostly  schistose 
on  the  Wisconsin  side  and  massive  on  the  Michigan  side.  This  fact  is 
indicated  on  Major  Brooks’s  map  and  speaks  strongly  against  the  view 
that  the  present  foliation  is  due  to  original  bedding. 

The  rock  of  the  exposure  which  occurs  farthest  down  the  river 
(Brooks’s  a)  outcrops  somewhat  less  than  a quarter  of  a mile  below 
the  bridge.  It  was  called  by  Wright  a chloritic  slate, 1 and  by  Wieh- 


1 Geol.  Wisconsin,  vol.  3,  j>.  712. 


124 


GREENSTONE  SCHIST  AREAS  OF  MICHIGAN. 


[BULL.  62. 


maim  a phyllite.  Major  Brooks  himself  designates  it  as  a “light  bluish 
gray,  shining  clay  slate , with  strong  cleavage  and  no  distinguishable 
bedding  planes.”1  It  does  not  beloug  to  the  rocks  now  especially  under 
consideration,  but  since  it  was  studied  carefully  it  may  be  described 
here  for  comparison.  This  slate  occurs  in  a bed,  estimated  by  Brooks 
to  be  550  feet  in  thickness,  on  both  sides  of  the  river  and  in  its  bed.  It 
strikes  nearly  east  and  west  and  dips  toward  the  north.  In  Brooks’s 
collection  this  rock  bore  the  number  2075 ; in  the  present  collection  it 
is  represented  by  No.  11152. 

Under  the  microscope  there  are  visible  in  the  thin  section  of  this 
specimen  unmistakable  signs  of  sedimentary  origin.  Coarser  and  finer 
areas  alternate,  the  former  being  made  up  of  clastic  quartz  grains, 
either  pure  or  mixed  with  iron  hydroxide  or  chlorite,  while  the  latter 
are  composed  of  an  argillaceous  substance,  filled  with  extremely  minute 
muscovite  or  sericite  scales  and  considerable  carbonaceous  matter. 
Tourmaline  needles  are  also  occasionally  seen  ; and  zircon  too,  either  in 
minute,  whole  crystals  or  as  irregular  fragments  of  larger  ones,  is  not 
infrequent.  This  rock  belongs  to  the  detrital  iron-bearing  series,  the 
boundary  between  which  and  the  greenstone  schists  lies  just  above 
this  exposure. 

The  railroad  which  crosses  the  bridge  at  Four-foot  Falls  exposes  this 
same  rock  again  in  a cutting  about  a mile  west  of  Iron  Mountain.  A 
specimen  from  this  locality,  No.  11114,  shows  the  same  general  charac- 
ter as  the  last  described  rock,  except  that  it  is  more  crystalline. 
Tourmaline  is  present  as  before,  but  anew  crystallization  of  biotite  has 
largely  replaced  the  chlorite.  The  carbonaceous  material  is  less  abun- 
dant and  what  remains  is  in  a much  more  finely  divided  state.  The 
clastic  origin  of  the  rock  is  still  very  apparent  in  the  shape  of  its  quartz 
grains,  which  are  here  mingled  with  feldspar  fragments,  both  plagio- 
clase,  microcline  and  orthoclase. 

No.  11113,  from  a quartzite  band  intercalated  in  No.  11114,  also  con- 
tains feldspar  grains  mingled  with  the  quartz.  Zircon  fragments  are 
likewise  present  and  a little  biotite,  which  is  no  longer  quite  fresh. 
This  latter  mineral  shows  in  a beautiful  manner  the  development  of 
secondary  rutile  needles,  as  in  the  kersantites.2 

Before  speaking  of  the  greenstones  which  occur  along  the  river 
farther  north,  it  will  be  well  to  examine  those  exposed  in  the  railroad 
cutting  at  the  western  end  of  the  bridge.  These  rocks  are,  for  the 
most  part,  massive,  but  they  nevertheless  display  evidence  of  extensive 
crushing  and  chemical  alteration.  No.  11178  represents  the  average 
type.  This  is  of  a light  green  color,  and  in  a hand-specimen  quite 
aphanitic.  Both  macroscopically  and  microscopically  it  resembles  the 
massive  greenstones  so  abundant  in  and  representative  of  the  region 
south  of  Marquette  (see  Pl.X,  fig.  2).  Miueralogically  there  is  hardly 
a trace  of  the  original  rock  left.  Almost  colorless  hornblende,  pale 


1 Geol.  Wisconsin,  vol.  3,  p.  475. 

2 Roseubusch : Mikros.  Physiog.,  2d  od.,  vol.  2,  p.  311. 


U.  S.  GEOLOGICAL  survey 


BULLETIN  NO.  62  PL.  VI 


THE  LIBRARY 
OF  THE- 

UHIYERSITY  OF  ILLINOIS 


Wlf.LIAMS.J 


GREENSTONES  NEAR  THE  FOUR-FOOT  FALLS. 


125 


green  chlorite,  zoisite,  leucoxene  and  a little  calcite  (all  of  secondary 
origin)  are  the  present  constituents;  and  yet  the  original  structure  of 
the  rock  is  strikingly  well  preserved.  When  viewed  with  a com- 
paratively low  power,  in  ordinary  light,  the  outlines  of  long,  almost 
acicular,  feldspar  crystals  are  very  apparent,  in  spite  of  the  fact  that  the 
substance  of  the  feldspar  itself  is  changed  to  chlorite  or  zoisite.  These 
outlines  of  former  crystals  make  a confused  aggregate,  but  each  indi- 
vidual preserves  its  own  proper  form  (idiomorphic  in  the  sense  of  Ros- 
enbusch).  The  angular  spaces  between  the  feldspars  produce  a typical 
example  of  the  ophitic  or  diabase  structure,  although  no  trace  of  a dia- 
base mineral  remains. 

But  the  exposure  is  not  throughout  as  massive  as  the  specimen  just 
described.  It  is  traversed  here  and  there  by  schistose  and  wavy  bands 
which  show  indications  of  having  been  much  crushed  and  rubbed. 
Slickensides  are  abundant  and  lenticular  fragments  fit  into  one  an- 
other so  as  to,  produce  an  imperfect  sort  of  foliation.  In  other  cases, 
where  the  crushing  has  been  more  intense,  the  schistosity  is  more  per- 
fect. These  bands  all  strike  a few  degrees  north  of  west,  being  appar- 
ently conformable  to  the  slates  below  and  the  greenstone  schists  above. 
This  is  a suggestivefact  when  it  is  remembered,  as  observed  by  Brooks, 
that  these  slates  owe  their  lamination  to  slaty  cleavage  (a  product  of 
pressure),  which  seems  to  have  obliterated  the  original  stratification. 

Ho.  11179,  from  one  of  the  schistose  bauds  in  the  greenstone  of  this 
cut,  shows  under  the  microscope  the  effects  of  great  mechanical  action. 
Curving  and  interlacing  areas  of  pale  green  chlorite  and  of  a grayish 
substance  (perhaps  the  remains  of  titanic  iron)  form  the  main  mass  of 
this  rock.  Thickly  scattered  through  these  are  patches  of  a dark  brown 
substance,  often  showing  concentric  zones  of  a clear,  transparent  char- 
acter. These  look  like  opal,  but  their  optical  character  shows  them  to 
be  single  individuals  of  crystalline  quartz.  Imbedded  in  this  material 
of  such  pronounced  secondary  character,  are  fragments  of  feldspar, 
which  have  been  crushed  or  broken.  These,  as  has  been  observed  so 
frequently  before,  are  less  changed  chemically  than  those  in  the  mass- 
ive rock  from  which  this  schistose  band  has  been  derived. 

Four  specimens  were  selected  to  represent  the  series  collected  along 
the  river  north  of  the  railroad  bridge.  Two  of  these  came  from  each 
side  of  the  river  and  illustrate  both  the  massive  and  schistose  bands. 

Ho.  11176  was  found  on  the  Michigan  (eastern)  side,  just  above  the 
bridge.  In  color  it  is  light  green,  and  in  structure  it  is  massive.  Under 
the  microscope  it  shows  a pale  hornblende  in  ragged  and  irregular  indi- 
viduals, feldspar,  zoisite,  chlorite,  and  leucoxene.  Traces  of  an  original 
diabase  structure  are  still  abundant  in  this  rock.  The  feldspars  often 
perfectly  preserve  their  lath-like  form  and  their  twinning  striation,  while 
the  pale  but  compact  hornblende  occupies  the  intervening  spaces,  sup- 
plying the  place  taken  by  the  augite  in  fresh  rocks  of  this  type. 

Ho.  11175,  from  the  highest  exposure  on  the  Michigan  side  of  Four- 


126 


GREENSTONE  SCHIST  AREAS  OF  MICHIGAN.  [bull.  62. 

foot  Falls,  is  quite  schistose  and  of  a much  darker  color  than  the  last 
rock.  Under  the  microscope  it  is  seen  to  possess  a much  finer  grain 
and  to  be  composed  of  hornblende,  chlorite,  feldspar,  quartz,  and  leu- 
coxene.  The  hornblende  is  for  the  most  part  pale  green,  but  that  it 
was  bleached  from  the  brown  variety  is  shown  by  the  numerous  com- 
pact brown  cores  which  occur  in  the  centers  of  the  paler  crystals.  The 
structure  of  this  rock  is  purely  granular,  with  no  trace  of  the  diabase 
type  which  characterized  the  specimen  last  described.  This  fact  and 
the  indication  that  the  pale,  fibrous  hornblende  was  derived  from  a 
compact,  brown  variety  of  the  same  mineral,  render  it  probable  that 
this  rock  was  originally  a diorite,  composed  of  feldspar  and  brown 
hornblende,  in  which  little  or  no  pyroxene  was  ever  present.  The  horn- 
blende of  this  rock  exhibits  a structure  quite  similar  to  that  described 
by  Becke1  and  Van  Hise2  as  due  to  a secondary  enlargement  of  the 
crystals  in  a solid  rock. 

The  accompanying  figure  represents  the  compact  brown  interior  of  a 
hornblende  individual,  more  or  less  sharply  separated  from  a pale  green 
or  colorless  border  of  hornblende  fibers,  which  possesses  exactly  the 
same  optical  orientation  as  the  core. 

Evidence  seems  to  be  constantly  ac- 
cumulating that  various  minerals 
may  continue  their  growth  by  regular 
accretions  in  solid  rocks,  whether  mas- 
sive or  clastic.  This  fact  is  satisfac- 
torily established  at  least  for  quartz, 
feldspar3  and  hornblende.  While  not 
in  the  least  doubting  the  correctness 
of  the  conclusions  above  cited  in  re- 
gard to  the  secondary  growth  of  horn- 
blende, I must,  however,  confess  that 
the  present  isolated  instance  appears 
to  me  hardly  to  offer  conclusive  proof 
that  the  fibrous  hornblende  border  is 
a secondary  crystalline  enlargement. 
Such  an  explanation  is  possible,  but 
the  appearance  can  be  equally  well  explained  in  my  judgment,  by  as- 
suming that  the  fibrous  zone  is  the  result  of  bleaching  and  fraying 
out  of  originally  compact  hornblende  crystals.  This  process  would 
naturally  commence  at  the  ends  of  the  crystals  and  develop  principally 
in  the  direction  of  the  cleavage,  as  is  here  seen  to  be  the  case.  The  only 
difficulty  with  this  explanation  is  the  sharp  line  sometimes  seen  between 
the  brown  and  the  fibrous  hornblende.  But  such  a sharp  boundary  is 
rather  the  exception  than  the  rule. 

•Tscherrnak’s  mineral,  u.  petrog.  Mittbeil.,  vol.  5,  1883,  pp.  158-59.  (cf.  Am.  Jour.  Sci.,  3d  series,  vol. 
33,  p.  385,  1887.) 

2 Am.  Jour.  Sci.  3d  series,  vol.  30.  p.  231,  Sept.  1885.  A.  Harker  has  also  recently  described  similar 
secondary  enlargements  of  hornblende  in  a hornblendcpicrite  from  Anglesey.  Geol.  Mag.,  London, 
3d  series,  vol.  4,  1887,  p.  550. 

3 See  Irving  and  Van  Hiso:  Bull.  U.  S.  Geol.  Survey,  No.  8. 


Fig.  19. — Compact  cores  of  hornblende  sur- 
rounded by  a fibrous  border,  No.  11175,  a schis- 
tose greenstone  from  Four-foot  Falls.  Mag- 
nified 180  diameters. 


WILLIAMS.] 


GREENSTONES  OF  THE  TWIN  FALLS. 


127 


Nos.  11142  and  11143,  taken  from  two  contiguous  bauds  on  the  Wis- 
consin side  of  the  river,  about  midway  between  the  two  points  which 
furnished  the  last  described  specimens,  represent  Brooks’s  localities  l and 
lc  respectively.  The  first  is  schistose,  the  second  massive.  The  first 
is  a pale  and  schistose  aggregate  of  nearly  colorless  chlorite,  light 
green  or  colorless  hornblende  fibers,  quartz  and  calcite.  The  second  is  a 
much  darker  green  mixture  of  feldspar,  hornblende,  chlorite  and  leu- 
coxene.  The  first  named  of  these  components  has  frequently  its  crys- 
tal form  well  preserved,  which  betrays  the  diabase  character  of  the 
mother  rock.  The  leucoxene  in  this  section,  as  well  also  as  in  Nos.  11175 
and  11176,  often  possesses  the  spliene-like  habit  which  has  been  figured 
from  No.  11189.  (PI.  XIII,  fig.  1.) 

THE  TWIN  FALLS. 

About  a mile  above  the  last  described  rock  exposure  at  the  so-called 
Four-foot  Fall,  the  quiet  course  of  the  Menominee  Fiver  is  again  inter- 
rupted by  a very  considerable  outcrop  of  greenstone.  This  is  almost  con- 
tinuous for  half  a mile,  but  at  either  end  of  it  the  river  plunges  over  a 
barrier  of  somewhat  harder  rock  than  usual  and  spreads  out  below  it 
into  a small  basin.  The  two  little  water-falls  thus  formed  are  known 
as  the  Twin  Falls.  In  Major  Brooks’s  report  they  are  included  in  the 
same  map  that  shows  the  topography  of  the  Four-foot  Fall,1  and  that 
portion  of  this  map  which  gives  the  outline  of  the  Twin  Falls  is 
reproduced  in  twice  the  scale  of  the  original  on  PI.  VI. 

All  of  these  exposures  belong  to  the  northernmost  of  the  two  green- 
stone belts  of  the  Menominee  Iron  Basin.  This  is  much  more  uniform 
in  its  composition  than  the  southern  belt,  in  which  the  Sturgeon  and 
Quinnesec  Falls  exposures  are  located.  Its  rocks  are  altogether  of  a 
dark  green,  almost  aphanitic  type,  which,  when  they  become  schistose, 
give  rise  to  dark  cliloritic  slates.  Neither  the  light  colored,  gabbro-like 
greenstone,  nor  coarse  diorites,  like  those  of  the  Horse  Face,  nor  bands 
of  acid  rocks  occur  in  the  northern  belt — at  least,  not  at  the  localities 
where  this  crosses  the  river. 

The  homogeneous  character  of  the  Twin  Falls  greenstones  is  largely 
due  to  an  advanced  state  of  chemical  alteration,  which  has  obscured 
its  original  grain. 

The  macrostruetural  changes,  whereby  the  compact,  dark  green  rocks 
are  converted  from  a massive  -to  a schistose  state,  may  be  admirably 
seen  along  the  river  banks  at  both  the  Upper  and  the  Lower  Twin 
Falls.  The  foliation  of  the  massive  and  already  chemically  altered 
rock  takes  place  in  a somewhat  different  manner  from  that  heretofore 
described.  There  are  none  of  the  ragged  u cross  gashes  ” and  irregu- 
lar, gaping  seams  (see  Fig.  10,  p.  81)  which  are  so  common  at  the  expos- 
ures along  the  southern  belt.  These  seem  to  be  the  result  of  stretch- 
ing in  a solid  or  very  nearly  solid  mass,  but  in  the  present  case  this 
process  is  hardly  apparent. 


Geol.  Wisconsin,  vol.  3,  p.  475,  PI.  IV. 


128 


GREENSTONE  SCHIST  AREAS  OF  MICHIGAN. 


[BULL.  62. 


The  first  step  toward  the  formation  of  a schistose  structure  in  these 
Twin  Falls  greenstones  (and  this  is  hardly  ever  absent)  is  the  division 
of  the  massive  rock  by  two  systems  of  joints,  which  stand  about  per- 
pendicular to  the  surface  and  intersect  at  a varying  but  acute  angle. 
These  joint  systems  divide  the  mass  into  diamond  shaped  or  rhomboidal 
prisms,  the  cross  sections  of  which  are  well  displayed  upon  the  fre- 
quent smoothly  glaciated  surfaces  of  the  rock.  The  appearance  of  such 
a surface  is  diagrammatically  represented  in  Fig.  20. 


Figs.  20-22  diagrams  illustrating  the  transition  from  jointing  to  schistose  structures  in  the  green 

stones  at  Twin  Falls. 

As  we  approach  the  schistose  band  in  the  massive  rock  these  inter- 
lacing rhombs  become  lengthened  out  more  and  more  by  an  approxima- 
tion to  parallelism,  between  the  two  systems  of  joint-planes.  (Fig.  21.1 


WlU.IAMS.l 


FOLIATION  PRODUCED  BY  SHEARING. 


129 


These  elongated  prisms  finally  become  very  much  extended  lenses, 
which  interlock  and  produce  a well  developed,  wavy  or  even  parallel 
schistose  structure  (Fig.  22).  The  almost  slaty  rocks  thus  produced, 
especially  as  seen  at  Lower  Twin  Falls,  have  a tendency  to  break,  not 
so  much  along  a definite  plane  as  parallel  to  a line — i.  e.,  the  direction, 
normal  to  the  surface,  parallel  to  which  the  original  joint  planes  ran. 
It  is  difficult  to  obtain  well  shaped  hand- specimens  of  these  rocks,  but 
narrow  rhombic  prisms  of  almost  any  angle  are  easily  procured.  There 
is  an  almost  equal  tendency  to  cleave  along  any  plane  which  is  parallel 
to  the  longest  axis  of  these  prisms. 

If  the  prisms  due  to  the  original  joint  planes  were  subjected  to  a lat- 
eral pressure  which  developed  in  them  a cleavage  that  successively  ap- 
proached more  and  more  nearly  to  the  long  axis  as  the  prism  was  length- 
ened, this  peculiar  tendency  to  separate  along  a line  rather  than  along 
a plane  is  precisely  the  structure  which  we  might  suppose  would  result. 

The  strike  of  these  schistose  bands  follows  the  direction  which  bisects 
the  acute  angle  of  the  rhombic  prisms.  This  is  for  the  most  part  from 
S.  70°  to  80°  E.,  agreeing  with  the  prevailing  strike  of  all  the  rocks  in 
this  system.  There  are,  however,  many  exceptions,  where  these  schistose 
bands,  even  where  near  together,  follow  different  directions ; for  in- 
stance, I observed,  in  the  massive  though  jointed  rock  on  the  Michigan 
side  of  Upper  Twin  Falls,  two  schistose  chloride  bands  quite  near 
together,  one  having  a strike  N.  180°  E.,  and  the  other  S.  73°  E.,  while 
the  dip  of  each  was  nearly  vertical.  Such  cases  are  easily  explicable  on 
the  supposition  that  these  bands  were  produced  by  mechanical  agencies, 
but  it  is  quite  impossible  to  reconcile  them  with  the  supposition  that 
these  bands  are  in  any  way  the  result  of  sedimentation. 

This  type  of  schistose  structure  was  also  noticed  to  a slight  extent 
at  some  of  the  exposures  of  the  lower  greenstone  belt — notably  just 
below  Lower  Quinnesec  Falls  on  the  Michigan  (left)  bank  of  the  river 
(see  p.  84).  It  is,  however,  there  the  exception,  and  is  peculiarly  the 
characteristic  of  the  upper  belt  as  exhibited  at  the  Twin  Falls. 

LOWER  TWIN  FALLS. 

The  development  of  the  foliation  in  the  massive  greeu stone  is  also 
shown  on  a small  scale,  partic- 
ularly on  the  left  (Michigan) 
side  of  Lower  Twin  Falls, 
where  there  has  been  a slight 
a mount  of  slipping  along  aline 
of  jointing.  Fig.  23  gives  a 
diagrammatic  idea  of  a speci- 
men observed  at  this  locality. 

The  area  represented  is  about 
three  feet  square.  Through 
the  center  runs  a vein  of  white 
quartz  which  has  been  depos- 
Bull.  62 9 


130  GREENSTONE  SCHIST  AREAS  OF  MICHIGAN.  [bull. 62. 

ited  by  infiltration  in  tlie  old  joint  seam.  On  the  edges  of  this  the  rock 
is  perfectly  schistose  and  chloritic,  but  it  passes  gradually,  in  the  space 
of  a few  inches,  into  the  massive  aphanitic  greenstone,  which  composes 
almost  all  of  this  exposure.  Fig.  24  represents  a polygonal  block, 
formed  by  the  jointing  of  the  massive  greenstone,  which  has  been 
frayed  out  into  a perfectly  foliated  chlorite  schist  by  a slipping  move- 
ment against  the  adjoining  blocks. 

The  extensive  chemical  alteration  which  has  gone  on  in  this  green- 
stone seems  to  render  it  peculiarly  sub- 
ject to  such  a fraying  out  into  a chloritic 
schist.  This  change  takes  place  in  cases 
where  a fresher  and  harder  mass  would 
have  received  only  a slickensides. 

The  Twin  Falls  greenstones  are  in- 
teresting, in  view  of  the  macrostructural 
alterations  which  they  exhibit.  Miner- 
alogically  they  are  all  so  much  decom- 
posed that  they  present  but  little  which 
is  determinable  under  the  microscope. 

The  least  altered  specimen  collected 
is  No.  11140,  from  the  east  side  of  the 
Lower  Fall.  Together  with  the  speci- 
mens shown  in  Figs.  23  and  24,  it  came 
from  a steep  wall  of  massive  and  but  little 
jointed  greenstone,  which  rises  abruptly 
from  the  water’s  edge.  Diamond  jointed 
and  somewhat  schistose  rocks  of  the 
same  sort  occur  on  the  north  (No.  11139) 
and  fissile  chloritic  slates  (striking  W.  of 
N.  and  dipping  70°  to  the  north)  to  the 
south  of  it.  Under  the  microscope  this 
massive  rock  is  found  to  be  a confused 
aggregate  of  pale  green,  somewhat  fib- 
rous hornblende,  feldspar  remnants,  and 
leucoxene,  which  possesses  a sphene-like  habit  and  rarely  shows  any 
trace  of  its  original  ilmenite.  The  clearer  areas,  which  represent  the 
former  feldspar,  are  now  so  filled  with  actinolite,  zoisite,  and  epidote 
needles,  that  nothing  regarding  the  former  character  of  this  mineral  can 
be  learned.  In  this  rock  secondary  biotite  is  also  quite  abundantly 
developed,  as  was  found  so  often  to  be  the  case  in  the  Russian  metamor- 
phosed diorites  described  by  Inostranzeff1.  The  original  structure  of 
this  rock  is  now  disguised  almost  beyond  recognition,  but  it  seems  to 
have  partaken  more  of  the  granular  nature  of  a diorite  than  of  the 
ophitic  nature  of  a diabase. 

No.  11132,  taken  from  the  continuation  of  this  mass  on  the  opposite 
JStudien  iibermetam.  Great.,  ©to.,  1879,  pp.  81,  82,  109-112. 


WILLIAMS.  1 


ANATASE  IN  ALTERED  DIABASE. 


131 


side  of  the  river,  is  essentially  identical  with  it,  but  in  it  the  form  of  the 
original  feldspars  is  better  preserved.  These  may.  often  be  seen  in 
well  formed,  lath-shaped  crystals,  which,  in  spite  of  their  extensive  saus- 
suritization,  still  retain  distinct  traces  of  their  plagioclastic  twinning 
striae.  This  rock  also,  in  distinction  from  the  one  last  described,  con- 
tains some  chlorite  but  no  biotite. 

These  rocks,  like  so  many  others  of  the  Menominee  River  greenstones, 
are  representative  examples  of  the  type  called  by  Giimbel  u Epidiorit,” 
which  is  now  generally  conceded  to  be  an  altered  form  of  diabase.1 

The  rocks  into  which  these  least  altered  forms  pass  are  representative 
chlorite  schists  and  slates ; and  there  can  be  no  doubt  that  these  latter 
have  also  resulted  from  the  extreme  effects  of  those  metamorphic  agen- 
cies which  changed  the  eruptive  diabase  to  the  epidiorite. 

No.  11130,  collected  just  below  No.  11132,  and  grading  imperceptibly 
into  it,  is  a schistose  rock,  composed  of  bright  green  chlorite,  finely 
granular  quartz  and,  perhaps,  second- 
ary albite.  The  leucoxene  m this 
rock  is  particularly  interesting.  It 
still  retains  small  ilmenite  cores  in 
places,  but  it  is  broken  and  pulled 
out  in  the  direction  of  the  schistosity. 

A very  considerable  portion  of  this 
leucoxene,  especially  around  the  edge 
of  the  grains,  is  composed  of  highly 
refractive  and  brightly  polarizing,  al- 
though extremely  minute,  colorless 
crystals.  These  have  an  octahedral 
habit  and  resemble  auatase  (Fig.  25), 
which,  as  both  Diller2  and  Eosen- 
busch3  have  shown,  sometimes  origi- 
nates fiom  the  alteration  of  ilmenite 
(cf.  also  Nos.  11050  and  11052  p.  121). 
tities  in  this  rock. 

- At  the  northwestern  corner  of  the  basin,  below  the  Lower  Twin  Fall 
(see  map  PI.  VI),  the  rock  is  rkomboidally  parted  and  weathers  to  a 
brownish  color.  In  spite  of  its  massive  appearance  it  possesses  a latent 
tendency  to  cleave  along  the  longest  diagonal  of  the  rhomboidal  prisms, 
and  this  tendency  is  intensified  by  weathering.  Toward  the  east  this 
rock  (No.  11128)  passes  gradually  into  corresponding  slates  (No.  11129). 
Under  the  microscope  these  two  rocks  are  seen  to  be  in  all  respects  the 
equivalents  of  Nos.  11132  and  11130,  above  described.  Their  main  dif- 
ference consists  in  their  being  richer  in  iron,  which  has  oxidized  and 


Fig.  25. — Auatase  derived  from  ilmenite,  No. 
11130,  from  the  Lower  Twin  Fall.  Magnified 
180  diameters. 


Biotite  also  occurs  in  small  quan- 


1 Cf.  Kosenbusoh  : Mikros.  Physio".,  2d  ed.,  vol.  2,  p.  205. 

2 Neues  Jahrbuch  fur  Mineral.,  1883,  vol.  1,  p.  191. 

3 Mikros.  Phyaiog.,  1st  ed.,  vol.  2,  1877,  p.  336;  2d  ed.,  vol.  1,  1885,  p.  332,  cf.  also  Schenck;  Inaugural 
Dissertation,  Bonn.,  1884,  p.  25. 


132 


GREENSTONE  SCHIST  AREAS  OF  MICHIGAN 


[BULL.  62. 


stained  the  rocks  brown.  No.  11128  still  retains  much  hornblende,  feld- 
spar, and  ilmenite,  and  the  diabase  structure  is  still  apparent  in  places. 
No.  11129  is,  like  its  counterpart  No.  11130,  a chlorite  schist  with  the 
hornblende  replaced  by  chlorite,  the  feldspar  by  a quartz  albite  mosaic, 
its  leucoxene  drawn  out,  and  its  structure  wholly  changed. 

Perhaps  the  most  altered  rock  of  any  encountered  at  the  Lower  Twin 
Fall  is  No.  11139,  which  was  one  of  the  chloritic  slates  on  the  Michigan 
side  of  the  river  below  the  massive  rocks.  This  is  a very  fine  grained 
aggregate  of  pale  green  chlorite,  quartz,  or  quartz  albite  mosaic  and 
biotite,  the  latter  constituent  being  sparingly  present.  Sharply  defined 
crystals  of  tourmaline  are  also  abundant  in  this  rock. 

UPPER  TWIN  FALLS. 

At  the  Upper  Twin  Fall  the  same  massive  greenstones  with  a rhom- 
boidal  parting  prevail,  everywhere  traversed  by  more  or  less  schistose 
bands.  No.  11133  is  the  massive  rock  from  the  left  or  Michigan  side 
of  the  fall.  It  is  much  altered  chemically,  but  preserves  its  original 
structure  almost  perfectly.  When  examined  by  a low  magnifying  power 
there  is  seen  a network  of  light  colored,  lath  shaped  feldspar  forms, 
which  are  almost  acicular,  like  those  of  a porphyrite.  Between  these 
is  an  allotriomorphic  mass  of  a dark  gray  substance,  representing  the 
former  augite,  or  possibly  a glassy  base.  When  examined  more  care- 
fully with  a higher  power,  the  feldspar  is  found  to  be  completely 
replaced  by  a mixture  of  pale  green  chlorite  and  brown  biotite  in  the 
closest  relationship,  while  in  them  an  occasional  crystal  of  zoisite  is 
imbedded.  The  darker  interstitial  mass  is  composed  largely  of  fibrous 
hornblende  in  shreds  or  confused,  matted  masses,  but  these  are  mingled 
with  much  impure  and  indeterminable  matter. 

Two  schistose  bandshave  already  been  mentioned  on  p.  129  as  travers- 
ing this  rock  in  different  directions.  Of  these,  the  one  striking  S.  73°  E. 
is  the  less  schistose,  and  is  represented  by  specimen  No.  11135.  Though 
much  more  altered  than  the  last,  there  are  here  also  occasional  unmis- 
takable traces  of  the  same  ophitic  structure.  The  representative  of  the 
other  band,  No.  11134,  is  hardly  more  than  a fine  schistose  aggregate 
of  chlorite,  quartz,  and  calcite,  with  only  the  faintest  indications  of  its 
original  structure,  and  yet  here  there  are  beautiful  leucoxene  borders 
around  unaltered  cores  of  ilmenite.  Narrow  veins  filled  with  a mixture 
of  calcite  and  chlorite  traverse  all  these  rocks. 

On  the  opposite  or  Wisconsin  side  of  the  Upper  Twin  Falls  the  rocks 
are  apparently  the  same,  but  they  show,  nevertheless,  important  mi- 
croscopic differences.  The  massive  forms  represented  by  Nos.  11122, 
11125,  and  11126,  collected  at  different  points  between  the  falls  and 
the  bridge,  are  fine  and  confused  aggregates  of  pale  green,  fibrous  horn- 
blende, chlorite,  zoisite,  quartz,  leucoxene,  and  occasionally  (No.  11122) 
a little  biotite.  All  of  these  minerals  are  of  secondary  origin  and  in 


Williams.] 


DIABASE  TUFFS  AT  UPPER  TWIN  FALLS. 


133 


the  process  of  their  formation  most  of  the  traces  of  the  former  rock- 
structure  have  been  obliterated.  Such  traces  as  still  remain  indicate 
that  the  mother-rock  was  a diabase,  but  there  are  seen  none  of  the  long, 
acicular  feldspar  forms,  discovered  in  the  rocks  from  the  opposite  side 
of  the  river. 

The  schistose  bands  interlaminated  with  these  rocks  are  quite  like 
those  already  described.  One  of  these,  however,  No.  11123,  obtained 
directly  beside  the  falls,  shows  almost  the  only  evidence  of  fragmental 
origin  anywhere  observed  in  the  Menominee  greenstones.  This  con- 
tains irregular  and  angular  fragments  of  quartz  and  a slightly  altered 
feldspar  of  considerable  size.  These  are  imbedded  in  a matrix  of  irregu- 
lar grain,  composed  of  chlorite,  calcite,  quartz,  and  opaque  iron  oxide, 
which  is  accompanied  by  leucoxene.  The  chlorite  scales  often  have  a 
radially  divergent  arrangement  around  the  larger  included  fragments 
of  quartz  and  feldspar. 

Thin  section,  No.  11122, shows  the  contact  of  this  schist  with  the  mass- 
ive rock.  This  contact  is  so  sharp  as  to  lend  much  additional  proba- 
bility to  the  idea  that  in  this  case  the  two  rocks  are  of  different  origin. 

Rocks  of  this  kind  are  to  be  regarded  as  diabase-tuffs,  similar  to  those 
which  are  so  largely  developed  around  Marquette,  and  which  are  to  be 
described  in  the  sequel.  It  is  easy  to  see  how  essentially  the  same  ma- 
terial, whether  produced  as  volcanic  ash  or  as  a massive  rock,  when 
subjected  for  a long  period  to  the  action  of  the  same  metamorphosing 
forces,  would  give  rise  to  masses  which,  in  certain  cases,  could  not  be 
distinguished  from  one  another.  This  is  undoubtedly  true  of  many 
occurrences  on  the  Menominee  River,  and  hence  we  can  speak  with  cer- 
tainty only  of  those  instances  where  sufficient  of  the  original  structure 
is  preserved  to  do  away  with  all  doubt.  Between  undoubted  massive 
rocks  rendered  schistose  by  pressure  on  the  one  hand,  and  fragmental 
tuffs  which  have  been  more  or  less  completely  solidified  by  the  same 
agency  on  the  other,  there  must  therefore  be  rocks  whose  original  form 
must  always  be  uncertain. 


CHAPTER  IV. 


— , 

GREENSTONE  BELTS  OF  THE  MARQUETTE  DISTRICT. 

INTRODUCTORY. 

a 

Ever  since  tbe  discovery  of  iron  in  the  northern  peninsula  of  Michi- 
gan, in  1844,  by  Burt  and  Houghton,  the  region  around  Marquette  has 
received  much  attention  from  geologists.  Although  not  eo  early  known 
as  the  famous  copper  district  of  Keweenaw  Point,  this  iron  region  has 
divided  the  scientific  interest  which  was  before  felt  in  the  copper- 
bearing  rocks. 

Douglass  Houghton,1  Locke,2  Foster  and  Whitney,3  Whittlesey,4 


Kimball,5  Credner,6  Brooks,7  Wright,8  Wadsworth,9  Rominger,10  and 
Irving11  have  studied  the  general  relations  of  the  deposits,  while  micro- 
scopical descriptions  of  some  of  the  rocks  have  been  given  by  Julien,12 
Wright,13  Wichmann,14  Pumpelly,15  Wadsworth,16  and  Irving.17 
The  city  of  Marquette  is  situated  on  the  south  shore  of  Lake  Supe- 


rior, about  midway  between  the  Carp  River  and  the  promontory  kuown 
as  Presqu’  Isle,  between  which  points  (a  distance  of  about  4 miles)  the 
lake  shore  runs  nearly  north  and  south.  The  city  for  the  most  part 
lies  within  the  square  mile  designated  as  Sec.  23,  T.  48  K.,  R.  25  W., 
Michigan. 

An  excellent  idea  of  the  topography  of  this  region  and  of  that  ex- 
tending for  18  miles  back  of  it  (i.  e.,  westward  from  the  lake)  may  be 
obtained  from  the  large  colored  map  prepared  by  Dr.  C.  Rominger.18 
- — — . 1 

I Brooks,  Geol.  Michigan,  vol.  1,  1873,  p.  13. 

2Geol.  Michigan,  vol.  2, 1873,  p.  239. 

3 Senate  Docs.,  1st  session,  30th  Congress,  1847— ’48,  II,  Doc.  2.  Report  on  the  Geology  and  Topog- 
raphy  of  the  Lake  Superior  Land  Dist.,  Part  II,  Iron  Region. 

4 Proc.  Am.  Assoc.  Adv.  Sci.,  1859,  vol.  xiii,  part  2,  pp.  301-308 ; ibid.,  1875,  vol.  24,  part  2,  pp.  60-72. 

6 Am.  J our.  Sci.,  2d  series,  vol,  xxxix,  1865,  pp.  290-303. 

6Zeitschr.  Deutsch.  geol.  Gesell,  vol.  xxi,  1869,  pp.  516-554. 

7 Geol.  Michigan,  vol.  1, 1873,  part  1.  pp.  1-319. 

8 “Geology  of  the  Lake  Superior  Iron  District’’  in  Swineford’s  History  and  Review  of  the  Copper, 
Iron,  Silver,  Slate,  and  other  Material  Interests  of  the  South  Shore  of  Lake  Snperior,  1876,  pp.  132-145. 

9Bull.  Mus.  Comp.  Zool.,  Cambridge,  vol.  7,  No.  1. 

10 Geol.  Michigan,  vol.  4,  part  x,  Marquette  Iron  Region,  1881,  pp.  1-154. 

II  Preliminary  paper  on  an  Investigation  of  the  Archean  Rocks  of  the  Northwest ; Fifth  Ann.  Rep. 

U.  S.  Geol.  Survey,  1886,  pp.  181-242. 

12Geol.  Michigan,  vol.  2, 1873,  Appendix  A. 

13  Geol.  Michigan,  vol.  2, 1873,  Appendix  C. 

14  “ Microscopical  Observations  of  the  Iron-bearing  (Huronian)  Rocks  from  the  region  south  of  Lake 
Superior,”  1876,  Geol.  Wisconsin,  vol.  3,  pp.  600-656. 

15  Am.  Jour.  Sci.,  3d  series,  vol.  x,  1875,  pp.  17-21. 

18  Bull.  Mus.  Comp.  Zool.,  vol.  7,  No.  1. 

17 Bull.  U.  S.  Geol.  Survey  No.  8,  pp.  27-30. 

18  Geol.  Michigan,  vol.  4, 1881,  in  pocket. 

134 


WILLIAMS.] 


THE  MARQUETTE  GREENSTONES. 


135 


The  general  trend  of  both  the  drainage  and  of  the  geological  forma- 
tions within  this  area  is  toward  the  east.  The  two  main  streams  follow 
somewhat  irregular  but  approximately  parallel  (eastward)  courses  and 
empty  into  the  lake  about  four  miles  apart.  The  more  northerly  of 
these  is  called  the  Dead  River ; the  more  southerly  the  Carp. 

The  general  surface  of  this  area  rises  by  degrees  from  the  level  of 
the  lake  to  an  elevation  of  about  1,000  feet  above  the  lake.  This  sur- 
face is,  however,  extremely  broken  and  hilly,  being  traversed  by  east 
and  west  ridges  composed  of  rows  of  rocky  knobs.  These  elevations  are 
never  over  two  hundred  feet  in  height  from  the  base  ; usually  they  are 
much  lower  (from  one  hundred  to  fifty  feet  or  even  less).  They  all  have 
rounded  outlines  produced  by  the  wearing  action  of  the  great  glacier, 
evidences  of  which  are  everywhere  apparent  in  the  smoothly  polished 
and  frequently  striated  rock  surfaces.  These  knolls  rise  from  the  even 
level  of  a plain  produced  by  the  glacial  debris  deposited  between  them. 

An  account  of  the  general  geological  structure  of  the  Marquette  region 
has  already  been  given  in  Prof.  Irving’s  explanatory  note  at  the  begin- 
ning of  this  paper,  in  which  is  included  also  a summary  of  the  different 
views  held  by  various  writers  with  regard  to  the  stratigraphical  posi- 
tion and  origin  of  the  rocks  of  the  greenstone-schist  area,  which  forms 
the  subject  of  this  part  of  the  present  essay.  In  connection  with  this 
account  has  also  been  given  a geological  map  of  the  Marquette  region, 
compiled  by  Professor  Irving  from  the  maps  of  Brooks  and  Rominger 
and  from  original  observations  of  his  own.  (PI.  I.)  It  will  not  there- 
fore be  necessary  for  me  to  present  anything  further  as  to  these  general 
matters  in  the  present  connection. 

Special  references  to  the  petrographical  work  of  others  on  the  Mar- 
quette rocks  will  be  made  in  the  course  of  the  following  detailed  descrip- 
tions. 

In  some  respects  the  greenstones  of  the  Marquette  area  seem  pecu- 
liarly suited  to  throw  light  upon  the  dynamic  metamorphism  of  basic 
eruptives,  since  a portion  of  these  rocks  seem  to  have  been  extruded 
both  during  and  subsequent  to  the  action  of  the  metamorphosing 
forces.  Hence  we  find  the  same  eruptives  in  different  stages  of  altera- 
tion. Moreover,  fragmental  material  (tuff)  of  the  same  nature  and 
origin  of  the  massive  rocks  is  abundantly  developed,  and  this  too 
shows  varying  stages  of  consolidation  into  masses  which  closely  re- 
semble the  solid  rock.  This  great  variety,  while  it  is  full  of  interest 
and  suggestions  of  new  possibilities,  is  frequently  very  confusing.  It 
often  becomes  impossible  to  speak  with  certainty  about  the  origin  of  a 
rock  which,  on  account  of  its  many  analogies,  we  may  regard  as  hav- 
ing been  produced  in  several  different  ways. 

The  general  similarity  of  the  greenstone  schists  of  the  Marquette 
and  Menominee  areas  will  be  brought  out  in  the  following  pages.  It  is 
worthy  of  mention  that  the  greenstone  schists  of  both  of  these  regions 
have  a strong  resemblance  to  some  of  the  greenstones  and  agglom- 


136 


GREENSTONE  SCHIST  AREAS  OF  MICHIGAN.  [bull.  62. 


erates  of  the  extensive  group  of  rocks  occurring  on  the  Lake  of  the 
Woods  and  on  Bainy  Lake  in  Canada,  to  which  Mr.  Andrew  0.  Law- 
son,  of  the  Canadian  Geological  Survey,  has  given  the  name  of  Kee* 
watin  series.  This  series  he  regards  as  belonging  immediately  be- 
neath the  Huronian,  which  is  represented  in  those  northern  regions 
by  the  so-called  Animike  series.1  This  is  also  the  position  which  the 
greenstone  schists  of  Marquette  occupy,  since  they  quite  unmistak- 
ably underlie  the  iron-bearing  detrital  rocks,  which,  according  to 
Irving,  are  the  equivalents  of  the  true  Huronian.  According  to  Irving 
also  the  greenstone  schists  here  probably  underlie  the  overlying  iron- 
bearing series  unconformably. 

The  Marquette  greenstone-schist  belt,  which  at  the  lake  shore  is 
between  2 and  3 miles  wide,  extends  to  the  westward  for  about  6 miles, 
without  materially  altering  its  form  or  width.  It  then  broadens  sud- 
denly by  a wide  extension  toward  the  north,  and  at  the  same  time  is 
divided  into  two  portions  by  the  eastern  extension  of  a narrow  arm  of 
granite  (See  map,  PI.  I).  The  southern  of  these  portions  continues  a 
due  westward  course  with  an  average  width  equal  to  that  of  the  entire 
belt  before  its  division.  The  northern  portion  is  separated  from  the 
southern,  first  by  granite,  and  then  to  a greater  and  greater  extent  by 
a large,  wedge  shaped  area  of  the  rocks  of  the  overlying  iron-bearing 
or  Huronian  series. 

For  convenience  in  arranging  the  following  petrographical  descrip- 
tions the  ground  covered  has  been  divided  into  four  areas,  which  will 
be  considered  in  order:  (1)  The  eastern  area,  near  Marquette;  (2)  the 
western  area,  immediately  north  of  Teal  Lake,  in  the  town  of  Negaunee ; 
(3)  the  northern  area,  lying  north  of  Dead  Biver,  and  (4)  the  Deer  Lake 
area,  a short  distance  north  of  the  town  of  Ishpeming.  The  last  named 
area  was  not  studied  by  the  writer  in  person,  specimens  from  it,  with 
full  descriptive  notes,  having  been  sent  to  him  by  Professor  Irving  for 
comparison  with  the  collections  which  the  writer  had  himself  made  in 
other  areas. 

In  the  eastern  or  Marquette  area  the  whole  width  of  the  greenstone 
belt,  including  the  granite  contact  on  the  north,  was  studied  for  a 
distance  of  3 miles  west  from  the  lake  shore.  In  the  western  or 
Negaunee  area  two  sections  were  run  northward  across  the  greenstone- 
schist  belt,  one  passing  through  Secs.  21,  28,  and  33,  T.  48  N.,  B.  26 
W. ; the  other  through  Secs.  13,  24,  25,  and  36,  T.  48  N.,  B.  27  W. 
In  the  northern  area  the  examinations  made  were  carried  on  from  a 
camp  situated  in  Sec.  9,  T.  48  N.,  B.  26  W.,  and  embraced  the  area 
covered  by  Secs.  3,  4,  5,  8,  9,  10,  and  11  of  this  township. 

The  first  of  these  areas  is  the  most  varied  in  its  petrographical 
characters,  and  it  was,  therefore,  the  most  thoroughly  studied.  It  is 

*See  General  Report  of  Progress  of  the  Geological  Survey  of  Canada  for  1885;  also  of  Am.  Jour. 
Sci.  (3d  series),  vol.  33,  1887,  p.  473.  I am  indebted  to  Dr.  Lawson  for  the  opportunity  of  examining 
the  extensive  suite  of  the  Rainy  Lake  rocks,  upon  the  microscopical  study  of  which  he  was  engaged 
in  the  petrographical  laboratory  of  Johns  Hopkins  University  in  the  winter  of  1886-’87. 


WILLIAMS.] 


DIVISIONS  OF  THE  MARQUETTE  AREA. 


137 


divided  into  two  portions  of  nearly  equal  extent  by  the  narrow  east 
and  west  band  of  iron-bearing  slates,  to  which  Rominger  applied  the 
name  of  Eureka  series.  The  northern  portion  of  the  Marquette  area, 
extending  from  Lake  street,  Marquette,  northward  to  the  granite,  is  in 
large  part  composed  of  banded  greenstone  schists,  having  an  east  and 
west  strike,  and  a steep  northern  dip.  They  are  most  conveniently  seen 
in  typical  development  on  Lighthouse  Point.  The  layers  of  these  rocks 
are  alternately  of  a darker  and  lighter  shade  of  green,  which  gives  these 
particular  greenstones  their  characteristic  striped  appearance.  In  these 
banded  rocks  of  the  northern  part  of  the  Marquette  area  intrusions  of 
comparatively  little  altered  acid  and  basic  matter  are  abundant.  These 
are  for  the  most  part  conformable  to  the  bedding  of  the  schists  and 
embrace  granites,  gneisses,  schistose  porphyries,  diorites,  and  diabases. 
Whenever,  in  these  undoubtedly  eruptive  rocks,  a schistose  structure 
is  apparent,  this  is  conformable  to  the  bedding  of  the  banded  green- 
stone schists. 

The  southern  portion  of  the  area  about  Marquette,  on  the  other 
hand,  is  occupied  by  much  more  massive  and  homogeneous  greenstones 
of  a nearly  uniform  light  green  color,  and  an  almost  aphanitic  struct- 
ure. These  are  characterized  by  their  division  into  oval  or  lenticular 
areas  which  interlace  and  which  are  separated  by  a finely  schistose 
material  of  much  finer  grain.  This  peculiar  parting,  which,  accord- 
ing to  the  writings  of  the  Canadian  geologists,  appears  to  have  a very 
widespread  distribution  through  the  greenstones  of  the  Northwest,  at 
first  glance  resembles  the  spheroidal  weathering  of  many  eruptive  rocks. 
There  is,  however,  better  reason  for  regarding  it  as  of  mechanical 
origin,  as  will  be  more  fully  explained  in  Chap.  V. 

The  schistose  structure  of  the  southern  Marquette  greenstones  is  of 
secondary  origin,  due,  probably,  in  almost  every  case,  to  pressure,  while 
anything  like  the  banding  or  striping  of  the  more  northern  rocks  is  here 
wholly  wanting.  Intrusive  rocks  are  rarer  than  in  the  banded  green- 
stones of  the  northern  portion  of  this  area.  When  such  dikes  do  occur 
they  are  much  more  altered  and  hence  approach  closely  to  the  enclos- 
ing rock — a fact  which  renders  their  detection  difficult. 

The  two  portions  of  the  Marquette  greenstone  area  are  therefore 
broadly  distinguished  in  many  of  their  petrographical  characters.  The 
east  and  west  band  of  iron  shales,  mentioned  above  as  separating 
them,  extends  from  the  north  side  of  Marquette  harbor  (Lake  street) 
westward  along  the  northern  side  of  the  Duluth,  South  Shore  and 
Atlantic  Railroad.  They  seem  to  be  identical  with  certain  members  of 
the  iron  series  and  at  one  point,  about  two  miles  west  of  Marquette,  they 
actually  contain  quite  an  extensive  deposit  of  hematite.  It  is  here 
that  the  Eureka  shaft  was  sunk  at  an  early  date  in  the  history  of  iron 
mining  in  the  Marquette  region,  and  from  this  Dr.  Rominger  has  taken 
his  name  for  this  series  of  Huronian  beds.  To  make  the  references  to 
localities  in  the  Marquette  area  more  intelligible,  a sketch  map  of  the 
environs  of  the  city  is  here  appended,  PI.  VII. 


138  GREENSTONE  SCHIST  AREAS  OF  MICHIGAN.  [bull. 62. 

With  reference  to  the  other  two  areas  examined  it  is  here  sufficient 
to  say  that  the  greenstones  of  the  western  or  Negaunee  area  more 
closely  resemble  those  exposed  in  the  southern  portion  of  the  Marquette 
region ; while  the  rocks  encountered  in  the  northern  area  show  many 
points  of  likeness  to  those  occurring  north  of  Marquette. 

ROCKS  OF  THE  NORTHERN  PORTION  OF  THE  MARQUETTE  AREA. 

BASIC  INTRUSIVES. 

Diabase. — Diabase  in  well  defined  dikes  of  various  sizes  is  an  impor- 
tant feature  in  the  geology  of  the  northern  portion  of  the  Marquette 
greenstone  area.  This  rock  occurs  in  all  stages  of  preservation  from 
an  unaltered  condition  to  a hardly  recognizable  aggregate  of  secondary 
and  decomposition  products. 

In  all  the  freshest  specimens  examined  olivine  is  present,  but  with 
the  commencement  of  alteration  this  mineral  is  the  first  to  disappear 
In  many  cases,  therefore,  where  the  rock  may  still  be  recognized  as  a 
typical  diabase,  it  is  now  impossible  to  say  whether  it  was  originally 
olivine-bearing  or  not. 

The  next  stage  in  the  alteration  is  marked  by  the  change  of  the 
pyroxene  to  uralite,  and  the  more  or  less  synchronous  passage  of  the 
feldspar  into  saussurite  and  of  ilmenite  into  leucoxene. 

Still  later  follows  the  development  of  such  final  decomposition  prod- 
ucts as  chlorite,  epidote,  calcite,  quartz,  etc.  The  extent  to  which  these 
chemical  changes  destroy  the  original  diabase  structure  differs  in  dif- 
ferent cases.  As  a rule  this  remains  distinct  during  the  first  two  stages 
of  alteration,  while  it  generally,  though  not  always,  disappears  during 
the  third.  In  some  instances  a pronounced  schistose  structure  has 
been  developed  in  undoubted  diabase  dikes  by  extensile  alteration. 

The  Great  Dike. — The  best  material  for  the  study  of  the  fresh  olivine 
diabase  near  Marquette  was  obtained  from  the  great  dike  which  forms 
the  center  of  Lighthouse  Point  (see  Pis.  I and  VII).  Here  its  eruptive 
character  may  be  admirably  seen  by  the  sharp  line  of  contact  which  it 
presents  with  the  adjoining  banded  green  schists.  This  dike  may  be 
traced  by  several  outcrops  along  Michigan  street  in  Marquette,  and 
then  as  a high,  rocky  ridge  which  extends  for  some  three  miles  westward, 
through  Sections  15  and  16,  just  north  of  the  main  road  from  Marquette 
to  Negaunee. 

From  various  portions  of  this  dike  nine  specimens  were  collected. 
The  four  freshest  of  these  specimens  (Nos.  11617  and  11622,  from  Light- 
house Point ; No.  11636,  from  Lighthouse  Point  quarry,  and  No.  11666, 
from  a cutting  on  Michigan  street)  are  not  to  be  distinguished  from 
one  another. 

The  structure  of  this  work  is  the  hyp-idiomorphic  diabase  struct- 
ure,1 which  forms  one  of  the  most  certain  characteristics  of  this  group 

^‘Structure  ophitique”  of  Fouqu6  and  Miehel-Levy,  “ Divergent-strahligkornige  Strnctnr  ” of 
Lossen,  and  “ Diabasischkdrnigo  Structur  ” of  Roaenbuscli. 


U.  S.  GEOLOGICAL  SURVEY 


BULLETIN  NO.  62  PL.  VII 


THE  LIBRARY 
OF  THE 

UNIVERSITY  OF  ILLINOIS 


wiuiAMs.)  DIABASE  OF  LIGHTHOlfSE  POINT  DIKE.  139 

of  eruptives.  The  grain  is  of  medium  coarseness.  The  lath-shaped 
plagioclase  crystals  measure  from  1.5  to  lmm  by  0.25  to  0.15mm.  The 
interstices  between  these  are  filled  with  augite  and  ilmenite.  The  min- 
eral components  observed  under  the  microscope  are,  in  order  of  their 
age,  as  follows : 

Essential ; Olivine,  labradorite,  augite,  \ Magnetite.  \ 

Accessory  : Apatite,  hornblende,  biotite,  quartz. 

Secondary : Serpentine,  uralite. 

The  olivine  is  mostly  in  rounded  grains  or  in  irregular  areas,  although 
it  sometimes  shows  evidences  of  a crystal  form,  especially  the  acute 
angle  due  to  the  intersection  of  two  dome  faces  (notably  in  No.  11666). 
It  is  commonly  wholly  changed  to  serpentine,  but  in  a few  instances 
remnants  of  the  original  transparent  olivine  substance  remain. 

The  feldspar  is  always  a plagioclase  with  the  peculiar  elongation  of 
the  crystal  in  the  direction  of  the  brachydiagonal  axis,  which  is  charac- 
teristic of  diabase.  The  crystals  are  always  striated,  often  minutely  so. 
The  extinction  is  generally  sharp,  although  an  undulatory  extinction 
is  sometimes  observed. 

The  augite  is  quite  normal  for  diabase.  It  is  of  a light,  slightly 
reddish  shade  of  gray,  with  a perfect  cleavage  parallel  to  the  prism. 
Twins  are  very  common,  and  the  line  of  the  lamellae  may  be  seen  in 
ordinary  light  traversing  the  basal  sections  and  bisecting  the  cleavage 
angles.  In  polarized  light  the  colors  distinguishing  the  twin  lamella? 
are  very  brilliant.  No  crystal  form  is  ever  recognizable,  the  mineral 
being  typically  “ xenomorphic,”  in  the  sense  used  by  Kohrbach.1 

Quartz  is  rare  in  diabase,  but  where  it  occurs  as  it  does  in  No.  11666 
we  must  regard  it  as  an  original  constituent,  on  account  of  the  extreme 
freshness  of  the  whole  specimen. 2 

The  iron  oxide  is  entirely  opaque  and  shows  a very  irregular  outline. 
This  is  mostly  due  to  the  penetration  into  it  of  the  feldspar  crystals 
whose  form  is  clearly  shown.  Its  crystallization  must  therefore  have 
been  subsequent  to  that  of  the  feldspar,  and  was  apparently  about 
synchronous  with  that  of  the  augite.  The  oxide  itself  is  probably 
partly  ilmenite  and  partly  a titaniferous  magnetite.  In  none  of  the 
freshest  specimens  does  it  show  trace  of  leucoxene.  It  is,  however, 
sometimes  partially  surrounded  by  a border  of  biotite. 

Original  hornblende  is  rare  in  this  rock,  but  traces  of  it  were 
observed  in  a few  instances. 

Among  the  alteration  products  serpentine  is  abundant  wherever 
olivine  existed,  but  the  rock  is  still  too  fresh  to  show  more  than  the 
most  occasional  uralitization  of  the  pyroxene. 

The  five  other  specimens  collected  from  this  great  dike  show  more 

1 Tsehermak’s  mineral,  u.  petrog.  Mittheil.,  vol  7,  1885.  Rolirbacli’s  two  terms,  “authomorphic’* 
and  “xonomorphic,”  adopted  by  Kalkowsky  (Litbologie,  1886,  p.  14)  wore  replaced  by  Rosonbusch  in 
the  last  edition  of  his  Massige  Gesteine  by  “ idiomorphio  ” and  “ allotriomorphic.”  though  for  what 
reason  is  not  apparent. 

2Cf.  Rosenbasch,  Mikros.  Physiog.,  2d  ed.,  vol.  2,  1886,  p.  188. 


140  GREENSTONE  SCHIST  AREAS  OF  MICHIGAN.  [bull.  62. 

altered  forms  or  abnormal  varieties  of  the  same  rock.  They  are  as 
follows : 

No.  11621,  glassy  diabase. 

No.  11675,  granophyre  diabase. 

No.  11672,  uralite  diabase  (structure  intact). 

No.  11615,  uralite  diabase  (structure  intact). 

No.  11610,  epidiorite  schist  (structure  gone). 

No.  11621,  collected  near  No.  11622  from  the  side  of  the  great  dike  on 
Lighthouse  Point,  is  a glassy  modification  of  the  diabase,  produced  by 
the  rapid  cooling  of  the  molten  mass  against  the  inclosing  walls.  The 
microscope  shows  this  rock  to  be  composed  of  a very  dark  brown  glass, 
which  can  be  rendered  transparent  only  with  the  greatest  difficulty. 
This  opacity  is  due  to  the  accumulation  of  minute  globulitic  bodies, 
which  can  be  detected  only  with  the  highest  magnifying  power  in  the 
thinnest  parts  of  the  slide.  Traces  of  the  arborescent  and  fern-like  forms 
common  in  basic  glasses  (tachylite)  are  easily  recognizable.  The  only 
mineral  constituents  which  have  crystallized  in  this  rock  are  olivine 
and  feldspar.  The  former  shows  well  defined  crystals.  These  fre- 
quently contain  inclusions  of  the  brown  glass,  and  are  now  wholly 
changed  to  a yellowish  green  serpentine.  The  feldspar  shows  the  nar- 
row, lath-shaped,  and  but  partially  completed  crystalloids  and  skeleton 
forms  which  abound  in  all  glassy  rocks.  These  are  filled  with  either 
penetrations  or  inclusions  of  the  brown,  glassy  base. 

The  chemical  constituents  of  the  other  diabase  minerals — augite, 
ilmenite,  etc.,  are  still  present  in  the  glass. 

No.  1167 5 presents  an  unusual  modification  of  this  diabase.  The  speci- 
men was  collected  from  the  high,  rocky  ridge  which  is  formed  by  the 
great  dike  in  the  southern  part  of  Section  16,  about  one  and  a half 
miles  west  of  Marquette.  The  hand-specimen  is  browner  than  is  usual 
in  this  diabase  and  is  speckled  with  reddish  spots.  Under  the  micro- 
scope the  grain  is  found  to  be  of  the  usual  coarseness  and  the  rock 
itself  slightly  more  altered  than  the  specimens  above  described. 

The  structure  of  the  rock  is  still  perfectly  preserved.  The  ilmenite 
is  unaltered,  and,  as  before,  is  frequently  fringed  with  biotite.  The  feld- 
spar is  clear  and  its  twinning  striations  are  very  distinct,  although  it  is 
traversed  by  many  interlacing  veins  of  a green  chloritic  alteration  pro- 
duct. There  are  no  certain  traces  of  olivine  in  this  rock  and  the  augite 
has  undergone  extensive  change  to  a brownish  yellow  hornblende. 
This  is  partly  fibrous,  but  also  in  part  quite  compact.  Indeed,  this  rock 
offers  a noteworthy  instance  of  the  apparent  change  of  augite  directly 
into  compact  brown  hornblende.  Much  more  of  this  mineral  is  here 
present  than  in  any  of  the  fresher  specimens  examined.  It  is  impossible 
to  assert  positively  that  some  of  it  did  not  exist  as  an  original  com- 
ponent of  the  rock,  but  the  frequent  cases  of  its  undoubted  derivation 
by  paramorphism  of  the  augite  makes  it  at  least  probable  that  all  the 
hornblende  has  originated  in  this  way. 

The  reddish  spots  spoken  of  as  visible  in  the  hand-specimen  represent 
another  interesting  feature  of  t hi ^ r.ick.  They  are  shown  by  the  micro* 


williams.]  ALTERED  DIABASE  OF  THE  GREAT  DIKE.  141 

scope  to  be  areas  of  a regular  intergrowth  of  feldspar  substance  and 
quartz.  This  is  sometimes  in  the  form  of  granophyre.  i.  e.,  in  slender 
fibers,  which  group  themselves  in  radiating  tufts  about  a clear  feldspar 
crystal,  and  sometimes  it  shows  the  structure  called  micropegmatite. 
This  latter  consists  of  small  angular  areas  of  quartz,  each  having  the 
same  optical  orientation,  which  are  embedded  in  the  reddish  globulitic 
feldspar  substance.1 

Quite  recently  Mr.  Waldemar  Lindgren  has  described  a similar  struct- 
ure in  a diabase  from  the  Big  Belt  Mountains,  Montana.2 

It  was  also  observed  by  the  writer  some  years  ago  in  a diabase  from 
Pleasant  Valley,  New  Jersey,  a specimen  of  which  he  received  from 
Mr.  J.  F.  Kemp,  of  Cornell  University. 

Rosenbusch3  regards  this  structure  as  sufficient  proof  that  the  quartz 
is  original,  but  the  observations  of  Irving4  in  the  Keweenawan  felsites 
and  others  make  this  conclusion  doubtful. 

No.  11672,  collected  at  the  corner  where  the  road  running  west  from 
Collins  Furnace  joins  the  road  leading  to  Bancroft  on  the  Dead  River 
(center  of  Sec.  17,  T.  48  N.,  R.  25  W.),  is  a uralite  diabase,  whose 
structure  is  still  perfectly  preserved. 

The  large  crystals  of  idiomorphic  feldspar  are  in  part  clear,  but  to 
a considerable  extent  clouded  by  the  development  of  saussurite. 

The  allotriomorphic  augite  is  in  some  cases  intact  or  remains  as  a 
core  in  the  center  of  the  secondary  hornblende  which  has  been  derived 
from  it.  More  frequently,  however,  the  hornblende  or  uralite  has  wholly 
replaced  the  pyroxene.  Its  structure  is  oftener  compact  than  fibrous, 
and  its  form  reproduces  exactly  that  of  the  original  augite.  Quartz 
areas  are  not  uncommon.  The  ilmenire  is  mostly  changed  to  leucoxene. 
Near  one  large  grain  of  the  latter  is  seen  an  area  of  brown  mica,  which 
is  filled  with  a sagenitic  network  of  minute  rutile  needles. 

No.  11615,  from  an  outcrop  of  this  same  great  dike,  at  the  bottom  of 
the  hill,  which  forms  the  eastern  end  of  Arch  street,  Marquette,  repre- 
sents the  next  stage  of  alteration  in  the  diabase. 

The  original  structure  is  still  plainly  recognizable,  although  it  is  be- 
ginning to  be  concealed  by  alteration. 

The  feldspars  exhibit  their  characteristic  lath-like  forms,  but  the 
sharpness  of  the  outlines  and  more  or  less  of  the  internal  substance  is 
clouded  by  secondary  products.  These  seem  to  be  for  the  most  part 
small  hornblende  needles  which  have  wandered  in  from  the  alteration 
of  the  pyroxene,  but  in  some  places  epidote  is  also  developed  from  the 
alteration  of  the  feldspar  itself.  Still,  in  nearly  every  case  enough  of 
this  unchanged  feldspar  is  present  to  show  plainly  its  original  form  and 
twinning  structure. 

'This  peculiar  structure  was  first  observed  in  diabase  by  Tornebolim  in  1877  (Neues  Jahrbuch 
fiir  Mineral.,  1887.  p.  262),  who  found  it  in  his  Konga-diabase  type  of  southern  Sweden,  and  named 
it  “ Schriftfeldspath.” 

2 Tenth  Census  Repta.,  U.  SM  vol.  15, 1887,  p.  736. 

* Mikros.  Physiog.  2d  ed.,  vol.  2. 

* Cf.  Mon.,  U.  S.  Geol.  Survey  vol.  5,  p.  114. 


142  GREENSTONE  SCHIST  AREAS  OF  MICHIGAN.  [bull.62. 

The  augite  is  in  the  process  of  changing  to  hornblende.  This  altera- 
tion is  sometimes  complete,  but  oftener  cores  remain  in  the  center  of 
what  was  the  original  pyroxene  crystal.  The  border  of  hornblende  is 
double,  consisting  of  a wider  internal  band  of  yellowish  brown  fibers 
which  have  apparently  resulted  directly  from  the  augite  substance,  and 
a narrower,  outer  zone  of  bright  emerald  green,  pleochroic  needles 
which  seem  to  project  into  the  surrounding  feldspar.1  The  individuals 
of  the  inner  zones  are  much  smaller  than  those  of  the  outer,  and  form 
a confused,  felt-like  mass,  while  the  external  needles  as  a rule  have 
their  longest  axes  parallel.  These  needles  are  most  developed  in  the 
direction  of  the  vertical  axis  of  the  augite.  They  may  owe  their  differ- 
ent coloring  to  the  influence  of  the  feldspar  substance  which  has  con- 
tributed to  their  formation.  In  some  cases  the  secondary  hornblende 
appears  to  be  homogeneous  over  considerable  areas,  exhibiting  a uni- 
form extinction  and  a comparatively  compact  character.  This  can  not, 
however,  be  regarded  as  original  in  its  nature. 

The  ilmenite  still  retains  its  form  but  is  largely  changed  to  leucoxene. 

No  traces  of  olivine  were  found  in  this  rock,  probably  because  of  its 
altered  condition. 

No.  11616  is  instructive  when  taken  in  connection  with  the  specimen 
last  described,  No.  11615.  Both  were  collected  from  the  large  and 
smoothly  glaciated  surface  of  trap,  exposed  at  the  east  foot  of  Arch 
street.  Through  the  massive  rock  run  a number  of  schistose  bands, 
produced  by  crushing  and  shearing  along  lines  of  weakness.  One  of 
these  bands  furnished  the  present  specimen.  There  can  be  no  doubt 
that  these  bands  are  a part  of  the  massive  rock.  Both  were  the  same 
before  the  schistose  bauds  were  produced  by  more  intense  mechanical 
and  chemical  action. 

Under  the  miscroscope  the  appearance  of  these  two  specimens  is 
found  to  accord  fully  with  their  field  relations.  Thb  original  diabase 
structure,  so  distinct  in  the  massive  rock,  has  wholly  disappeared  in  the 
schistose  one.  There  are  no  traces  of  lath-shaped  feldspar  left.  The  rock 
is  mainly  composed  of  a confused  network  of  fibrous,  very  pale  green 
and  slightly  pleochroic  hornblende  needles.  These  are  sufficiently  par- 
allel in  their  arrangement  to  produce  the  schistose  structure  of  this 
rock.  They  are  secondary — formed  from  the  alteration  of  the  augite  or 
the  joint  alteration  of  the  pyroxene  and  feldspar — as  maybe  admirably 
seen  in  section  No.  11615,  where  they  are  in  the  process  of  formation. 
Scattered  among  this  hornblende,  is  considerable  cloudy  and  nearly 
opaque  saussuritic  substance,  mixed  with  more  or  less  secondary  quartz, 
both  of  which  have  been  derived  from  the  feldspar.  The  ilmenite  also 
has  undergone  an  interesting  alteration  and  is  here  represented  by 
cloudy  leucoxene,  with  only  occasional  opaque  black  dots  of  the  origi- 
nal mineral.  This  substance  is  arranged  in  long  stringers  and  shreds 
which  follow  the  direction  of  the  schistose  structure. 

'On  the  production  of  a similar  double  uralit©  zone  around  pyroxene.  See  Lessen : Erliiut.  z.  geol. 
Specialkarte  von  Preuaaen  u.  d.  tliiiring.  Staaten,  Blatt  Harzgerode,  p.  81, 1882 ; and  Williams;  Bull 
U.  S,  Geol.  Survey,  No.  28,  p.  42,  PI.  I,  Fig.  2. 


WILLIAMS.] 


THE  BROOK  SECTION. 


143 


Here  we  have  an  undoubted  instance  of  the  dynamic  metamorphism 
of  a diabase,  where  every  stage  in  the  process  can  be  followed.  Every 
mineral  of  the  schist  can  with  certainty  be  traced  to  its  original  form, 
and  yet  the  chemical  alteration  has  been  accompanied  by  such  a change 
of  position  (migration)  that  the  original  structure  has  wholly  disappeared 
and  a new  and  different  structure  has  been  produced.  This  derived 
rock  is  quite  identical  with  some  of  the  most  characteristic  so-called 
hornblende  or  actinolite  schists. 

The  chemical  action  has  here  been  proportionately  increased  by  the 
crushing.  This  seems  true  for  all  the  constituents,  as  there  are  no 
traces  of  the  fresh  fragments  of  broken  feldspar  crystals  which  were  so 
often  observed  in  analogous  greenstones  of  the  Menominee  region. 

There  is  an  excellent  section  through  the  rocks  of  the  northern  por- 
tion of  the  Marquette  area,  exposed  by  a brook  which  flows  northward 
almost  along  the  line  between  Sections  15  and  16  (hardly  over  a mile 
west  of  the  city)  and  empties  into  Dead  River.  Between  the  road  lead- 
ing from  Marquette  to  Collins’s  Furnace  and  that  forming  the  main  high- 
way toNegaunee,  this  small  stream  has  excavated  a deep  ravine,  upon 
the  high,  steep  sides  of  which  the  relationship  of  the  different  rocks  is 
admirably  diplay ed.  This  locality  is  described  by  Dr.  Rominger,1  and 
for  convenience  we  will  in  future  allude  to  it  as  the  Brook  section. 
(See  PI.  VII.) 

Here  were  encountered  several  exposures  of  fresh  olivine  diabase. 
One  of  these,  No.  11708,  was  taken  from  the  branching  dike  in  the 
wall  of  greenschist  and  granite,  which  Rominger  has  described  and 
figured.2  This  rock  resembles  the  freshest  specimens  obtained  from 
the  great  dike,  except  that  its  grain  is  finer,  as  might  be  expected  in 
a mass  of  so  much  smaller  size.  No  trace  of  alteration  is  here  visi- 
ble, except  in  the  olivine.  This  constituent  is  not  abundant,  but  it 
occasionally  appears  in  well  shaped  crystals,  which  are  completely 
changed  to  yellow  serpentine.  The  iron  oxide  presents  in  its  form  a 
decided  contrast  to  that  above  described.  In  this  rock  it  was  produced 
much  earlier  than  in  the  other,  and  hence  it  has  a well  developed  crystal 
form.  This,  as  seen  under  the  microscope,  is  square  (octahedral  section), 
which  may  be  an  indication  that  the  mineral  is  magnetite  instead  of 
ilmenite,  as  before.  The  feldspar  and  pyroxene  of  this  rock  need  no 
special  comment. 

No.  11719,  obtained  near  the  edge  of  another  dike  not  far  from  the 
last  mentioned  one,  is  only  semi-crystalline.  Its  brown,  glassy  base  re- 
sembles that  of  No.  11621,  but  crystallization  is  farther  advanced.  The 
sharply  defined  olivine  and  feldspar  crystals  are  quite  the  same,  but  a 
vast  number  of  smaller  feldspar  crystals  are  here  developed  in  the  base. 
Only  a very  little  augitc,  and  that  in  rounded  grains,  is  present.  This 
rock  would  be  correctly  termed  a raelaphyre. 


•Geol.  Michigan,  vol.  4.  p.  25, 
‘Ibid.,  p.  148. 


144 


GREENSTONE  SCHIST  AREAS  OF  MICHIGAN. 


[BULL.  62. 


No  11679  is  from  the  center  and  No.  11680  from  the  edge  of  a dike 
of  porphyritic  greenstone,  which  intersects  the  banded  green  schists  on 
the  western  side  of  the  Brook  section,  not  far  from  its  southern  end. 

The  first  of  these  rocks  has  a coarsely  porphyritic  structure,  which, 
on  account  of  its  altered  condition,  is  only  prominent  on  a weathered 
surface.  A fresh  fracture  appears  of  an  almost  even  gray  color,  re- 
sembling some  of  the  finer  greenstones.  Under  the  microscope  this 
specimen  is  found  to  correspond  admirably  to  the  descriptions  of 
the  rock-type,  named  by  Giimbel  “ epidiorite.”  The  augite,  reddish 
brown  cores  of  which  still  remain,  is  largely  changed  to  fibrous  horn- 
blende. This  mineral  is  mostly  of  a pale  brown  color,  but  often  has  a 
bright  green  edging  where  it  adjoins  the  feldspar  substance,  as  has 
already  been  noted  in  the  case  of  No.  11615  (p.  141).  The  feldspar  is 
still  clear  and  fresh,  showing  the  characteristic  lath-shaped  forms  of 
diabase.  It  is  only  rarely  clouded  by  small  patches  of  a gray  saussurite. 
Much  more  abundant  in  this  feldspar  are  veins  and  small  areas  of  green 
hornblende  needles,  which  owe  their  existence  mostly  to  the  pyroxene, 
though  the  feldspar  seems  also  to  have  aided  in  their  formation.  They 
are  especially  abundant  in  cracks,  along  which  the  substance  appears 
to  have  wandered  from  the  decomposing  augite.  This  hornblende  is 
finely  fibrous  and  forms  matted,  felt- like  masses.  There  is  but  little 
chlorite  and  secondary  quartz  in  this  rock.  The  ilmenite  is  largely 
changed  to  leucoxene  and  occasionally  surrounded  by  a rim  of  biotite. 

The  second  of  these  two  specimens  (No.  11680)  from  the  edge  of  this 
dike,  shows  an  extremely  fine  grained,  greenish  groundmass,  whose 
components  are  very  weakly  polarizing  and  hardly  determinable.  This 
was  perhaps  once  a glass  which  has  become  devitrified  and  viriditic. 
In  it  are  imbedded  sharp,  lath-shaped  plagioclase  crystals,  which  are 
either  unaltered  or  at  most  penetrated  by  veins  of  actinolite  needles, 
and  augite  almost  wholly  changed  to  hornblende  or  chlorite. 

The  following  five  rocks  are  also  good  representatives  of  the  epidio- 
ritic  type.  They  are  largely  composed  of  either  light  or  dark  green, 
fibrous,  secondary  hornblende.  In  none  of  them  does  any  trace  of  au- 
gite now  remain,  and  it  is  possible  that  some  of  them  were  originally 
true  diorites,  like  the  rocks  to  be  described  under  the  next  head.  How- 
ever, the  unmistakable  evidences  of  diabase  structure  often  apparent 
render  it  more  probable  that  these  rocks  all  belonged  originally  to  this 
type. 

No.  11663,  from  Pine  street  just  north  of  Michigan  street,  Marquette, 
is  most  like  a true  diorite  and  may  be  an  altered  form  of  the  Picnic  Isl- 
and rock.  The  hornblende  is  of  the  general  type  represented  in  PI.  XII, 
fig.  2 of  No.  11186,  from  the  Horse  Race  above  Upper  Quinnesec  Falls 
(see  p.  107).  It  is  more  or  less  fibrous,  of  a pale  green  color  and  often 
looks  as  though  it  had  originated  from  the  bleaching  and  disintegration 
of  a compact  original  hornblende.  Around  the  edge  of  large  areas  it 
has  a darker  green  border  and  seems  to  ravel  out  into  fine  fibers  which 


WILLIAMS.  ] 


EPIDIORITES. 


145 


wander  into  the  feldspar.  Indeed,  the  feldspar  is  quite  filled  with  such 
hornblende  needles,  which,  together  with  its  saussuritic  alteration  prod- 
ucts, almost  conceal  the  original  substance.  Ilmenite  in  ragged  areas, 
but  without  leucoxene,  and  a little  of  the  chlorite-epidote  aggregate  (see 
PI.  XI,  fig.  1)  are  also  present. 

Nos.  11712  and  11720,  both  from  the  Brook  section,  are  rocks  of  the 
same  general  character  as  that  last  described.  The  former  is  decidedly 
schistose  and  bears  much  internal  evidence  of  the  action  of  great  press- 
ure. All  of  the  constituents  are  arranged  in  interlacing  and  elongated 
bands.  The  feldspar  is  much  crushed  and  shows  the  peculiar  mosaic 
due  to  secondary  crystallization.  It  is  also  often  changed  to  a granular 
aggregate  of  brightly  polarizing,  pale  green  epidote  grains.  The  horn- 
blende crystals  are  broken  and  bent,  and  especially  around  their  outer 
edge,  are  very  frequently  reduced  to  a confused  mass  of  fine  needles 
which  have  extensively  wandered  out  into  the  feldspar  substance.  The 
ilmenite  also  is  much  crushed  and  elongated  in  the  direction  of  the  schist- 
osity,  but  it  shows  no  indication  of  being  changed  to  leucoxene. 

The  second  specimen,  No.  11720,  is  somewhat  schistose,  though  less 
so  than  the  last.  It  is  extremely  dark  in  color  owing  to  the  large  pro- 
portion of  iron  which  enters  into  its  composition.  Under  the  microscope 
it  is  a confused  aggregate  of  very  dark  green  and  strongly  pleochroic 
hornblende  needles,  a little  feldspar,  proportionately  much  ilmenite  and 
quartz.  Some  of  the  larger  hornblende  crystals  show  the  peculiar  granu- 
lated center,  lately  described  and  figured  by  me  from  the  gabbro-diorites 
occurring  near  Baltimore,1  to  which  indeed  this  specimen  presents  many 
points  of  close  resemblance. 

The  two  remaining  specimens  are  much  more  altered  than  those  just 
described. 

No.  11661,  found  beside  the  granite  boss  (the  so-called  “gold  mine”) 
just  west  of  Pine  street,  Marquette,  is  coarsely  granular.  The  feldspar 
is  altered  to  saussurite  or  calcite.  The  hornblende  is  pale  green  and 
partly  fibrous.  The  center  of  the  crystals  is  frequently  composed  of  a 
dark,  yellowish  green  substance  which  hardly  polarizes  at  all.  This,  at 
first  glance,  appears  to  be  a core  of  compact  brown  hornblende  but  a 
closer  examination  shows  that  this  is  not  its  nature.  A little  sphene 
and  considerable  blood  red  iron  hydroxide  make  up  the  remainder  of 
this  rock. 

The  last  specimen  of  these  epidioritic  rocks,  No.  11711,  was  part  of 
a well  marked  dike  of  schistose  greenstone  which  intersects  a boss  of 
gneiss  near  the  northern  end  of  the  Brook  section.  This  gneiss  strikes 
E.  and  W.,  while  the  dike  strikes  N.  75°  E.  The  schistosity  of  the 
latter  is  parallel  to  its  walls,  so  that  the  foliations  of  the  two  rocks 
intersect  at  an  angle.  This  rock  shows  the  effects  of  pressure  and 
crushing.  It  is  now  a finely  granular  aggregate  of  pale  green  fibrous 
hornblende,  feldspar,  quartz,  calcite,  and  leucoxene. 

1 Bull.  TJ.  S.  Geol.  Survey,  No.  28,  p.  28,  PI.  Ill,  fifc.  1. 

Bull.  62 10 


146 


GREENSTONE  SCHIST  AREAS  OF  MICHIGAN. 


[BULL.  62. 


Diorite. — The  occurrence  of  typical  original  diorite  in  the  Marquette 
area  still  seems  a little  doubtful.  No.  11654,  which  composes  the  Picnic 
Islands,  a short  distance  north  of  Lighthouse  Point,  comes  nearest  to 
deserving  this  name,  although  this  rock  might  with  as  much  propriety 
be  termed  an  amphibole  granite.  Julien  called  it  a u quartzose  porphy- 
ritic  diorite,”1  and  he  was  followed  by  Wadsworth.2  The  microscope 
shows  this  rock  to  be  a coarsely  granular  aggregate  of  green  horn- 
blende, saussuritized  plagioclase,  together  with  a less  altered,  unstriated 
feldspar,  quartz,  and  sphene.  The  hornblende  is  mostly  quite  com- 
pact, and  shows  in  cross-section  sharp  crystalline  outlines,  which  are 
often  twinned.  The  plagioclase  contains  large  zoisite  individuals  aside 
from  its  more  usual  saussurite  aggregate.  The  unstriated  feldspar 
seems  to  alter  to  muscovite  or  kaolin,  as  is  common  in  orthoclase. 
Seams  in  this  rock  are  filled  with  epidote,  calcite,  or  more  rarely  specu- 
lar iron. 

The  Picnic  Island  rock  seems  to  be  most  closely  related  to  the  amphi- 
bole-granites,  gneisses,  diorites,  and  massive  hornblendite  which  occur 
in  the  granite  farther  north — notably  on  Partridge  or  Middle  Island, 
beyond  Presqu’  Isle.  At  this  latter  locality  there  is  every  evidence, 
from  the  intimate  association  of  the  granite  and  these  hornblendic 
rocks,  that  they  were  both  liquid,  or  at  least  plastic,  at  the  same  time. 
Such  a perfect  intermingling  of  the  two  magmas  it  seems  impossible 
to  explain  on  any  other  hypothesis ; nor,  indeed,  are  indications  of  the 
same  intermingling  wanting  on  some  of  the  Picnic  Islands. 

ACID  INTRUSIVES. 

General  character. — The  association  of  acid  rocks  of  various  types 
with  the  greenstones  of  the  northern  portion  of  the  Marquette  area  is 
not  less  intimate  than  that  already  described  as  occurring  at  Upper 
Quinnesec  Falls,  on  the  Menominee  Eiver.  (Chap.  Ill,  p.  110.)  The 
general  character  of  these  rocks  is  very  similar  at  both  localities,  and 
at  both  they  offer  equally  valuable  material  for  the  study  of  dynamic 
metamorphism. 

The  passage  from  the  Marquette  greenstones  to  the  granite  lying 
north  of  them  is  an  extremely  gradual  one.  There  is  no  such  sharp 
line  of  contact  as  is  represented  on  RomingePs  map,  but,  on  the  con- 
trary, as  Rominger  himself  explains,  there  is  a complete  interpenetration 
of  the  two  rock  masses.  The  granite  has  intruded  itself  into  the  schis- 
tose greenstones,  for  the  most  part  following  their  bedding  and  forcing 
apart  their  strata.  The  amount  of  the  acid  rock  gradually  diminishes 
as  we  go  southward.  At  the  Dead  River  it  still  composes  over  half 
of  the  entire  mass,  but  between  this  and  the  city  of  Marquette  the 
dikes  and  bosses  of  granite  grow  less  and  less  frequent.  They  are, 

•Geol  Mich.,  vol.  2,  p.  163. 

2 Notes  on  the  Iron  and  Copper  Rocks  of  Lake  Superior.  Bull.  Mus.  Comp.  Zool.,  Harvard  Coll. 
Whole  Series,  vol.  7,  Geol.  Series,  vol.  1,  p.  39. 


WILLIAMS.] 


THE  GRANITE  OF  DEAD  RIVER. 


147 


however,  never  entirely  absent  from  the  northern  part  of  the  green- 
stone area,  but  extend  to  the  limits  of  the  Eureka  series.  Around 
Lighthouse  Point  and  near  the  Marquette  water- works,  on  the  north 
side  of  the  harbor,  bands  of  reddish  and  gray  acid  rocks  may  be  seen 
along  the  lake  shore  in  abundance.  Some  of  these  are  but  little  altered 
granites  and  porphyries,  while  others  are  decidedly  schistose  and  seem 
to  owe  their  structure  to  dynamic  agencies. 

Granite . — We  will  first  examine  specimens  of  the  unaltered  granitic 
type.  These  can  be  nowhere  better  seen  than  in  the  neighborhood  of 
the  powder  mill  on  Dead  River,  near  the  center  of  Section  10.  Near 
this  place  were  obtained  Nos.  11612  and  11613,  both  normal  granites 
which  penetrate  the  schistose  greenstones.  They  are  of  a reddish 
color  and  consist  principally  of  feldspar  and  quartz,  both  of  which  are 
allotriomorphic  and  form  a granular  aggregate  of  interlocking  grains. 
The  quartz  areas  are  often  composite,  and  are  traversed  by  lines  of 
fluid-cavities,  containing  movable  bubbles,  The  feldspar  is  both  mon- 
oclinic and  triclinic.  It  is  considerably  altered  to  muscovite  or  kaolin. 
A little  chlorite  represents  the  original  presence,  in  small  quantity,  of 
a third  constituent,  but  its  condition  is  now  too  much  altered  to  allow  of 
its  exact  determination.  The  second  of  the  two  specimens  (No.  11613) 
is  the  coarser  grained  and  contains  both  microcline  and  pyrite,  which 
are  lacking  in  the  former. 

No.  11668,  also  from  near  the  powder  mill,  occurs  where  the  granite 
and  schistose  greenstones  are  very  intimately  associated  and  it  seems 
to  be  intermediate  between  them.  Under  the  microscope  it  appears  as 
a reddish  granite,  like  those  last  described.  Apatite  crystals  and  mi- 
nute, sharply  defined  zircons  are  abundant.  The  greenish  color,  which 
imparts  to  this  rock  an  appearance  intermediate  between  a granite  and 
a greenstone,  is  due  to  the  large  amount  of  chlorite  present.  This 
sometimes  traverses  the  feldspar  in  irregular  veins  and  is  sometimes 
massed  together  in  larger  areas,  as  though  it  had  resulted  from  the  al- 
teration of  some  bisilicate,  or,  as  is  still  more  probable,  of  a micaceous 
constituent. 

Toward  the  southern  end  and  on  the  west  side  of  the  Brook  section, 
the  banded  greenstones  and  granite  are  exposed  in  relations  not  less 
interesting  than  those  to  be  seen  at  Dead  River.  A large,  glaciated  sur- 
face of  the  schists  shows  intrusions  of  both  granite  and  diabase  which 
cut  directly  across  the  strike.  The  former  rock  contains  angular  frag- 
ments of  the  schist  and  in  one  case  it  fills  the  inequality  formed  by  the 
faulting  of  the  schist  along  a joint  plane  nearly  perpendicular  to  its 
bedding.  It  also  forms  narrow  veins  and  rows  of  bulging  lenses  in  the 
schist.  This  granite  shows  no  signs  of  foliation  in  the  field,  but  a closer 
study  of  it  in  the  laboratory  discloses  the  effects  of  powerful  dynamic 
action.  The  hand-specimen,  No.  11678,  proves  upon  microscopical  ex- 
amination to  be  an  excellent  example  of  peripheral  granulation,  pro- 
ducing whatTornebohm  has  called  the  u mortar-structure.”  The  grains 


148 


GREENSTONE  SCHIST  AREAS  OF  MICHIGAN. 


[BULL.  62. 


have  rubbed  against  one  another  and  formed  a fine  mosaic— mostly  a 
new  crystallization — which  resembles  a cement.  The  quartz  has  suf- 
fered so  much  by  this  process  that  hardly  a trace  of  the  original  granitic 
quartz  remains.  The  feldspar  presents  rounded  grains,  often  bent  or 
fissured.  In  the  cracks  thus  formed  the  same  mosaic-like  cement  is 
developed.  Chlorite,  epidote,  muscovite,  and  iron  hydroxide  are  present 
in  this  fine  grained  mass  between  the  rounded  feldspars. 

No.  11710  was  obtained  from  the  rounded  knob  of  gneissoid  granite, 
near  the  northern  end  of  the  Brook  section,  through  which  the  dike  of 
foliated  trap  described  on  p.  145  (No.  11711)  passes.  In  this  rock  the 
gneissic  structure  is  quite  prominent  through  a parallel  arrangement  of 
the  constituent  minerals,  but  under  the  microscope  it  quite  closely  re- 
sembles the  last  specimen.  The  same  peripheral  granulation  of  the 
original  graius  by  rubbing  is  even  more  apparent ; and,  although  there 
is  no  marked  tendency  to  parallel  arrangement  visible  in  the  thin  sec- 
tion, the  effects  of  pressure  are  everywhere  shown,  as  in  the  undulatory 
extinction  of  the  quartz,  in  the  production  of  secondary  strain-lamellae 
in  the  feldspar,  and  in  the  presence  of  microcline. 

No.  11614  was  obtained  from  a gray  granitic  knob  on  the  lake  shore 
at  the  mouth  of  Dead  River.  This  is  penetrated  by  several  sharply 
defined  dikes  of  fine  grained  diabase,  and,  like  the  rock  last  described, 
is  decidedly  gneissoid  in  structure.  The  rock  is  composed  mainly  of 
quartz  and  orthoclastic  feldspar,  although  both  plagioclase  and  a green 
fibrous  hornblende  are  also  present.  The  gneissic  or  u flaser  ” structure 
is  its  most  striking  feature.  This  is  plainly  visible  in  the  thin  section 
and  seems  to  be  mainly  due  to  the  elongation  of  the  quartz  areas  in 
the  direction  of  the  foliation.  This  mineral  has  suffered  greater  defor- 
mation than  the  feldspar  and  is  present  in  long,  lenticular  patches* 
whose  axes  are  often  sinuous.  These  are  for  the  most  part  composite 
and  always  show  an  undulatory  extinction.  There  is,  strangely  enough, 
no  peripheral  granulation  visible  in  this  rock. 

No.  11660  is  from  a granite  boss  on  the  west  side  of  Pine  street,  north 
of  Ohio  street,  Marquette.  A fine  section  has  recently  been  laid  open 
through  the  center  of  this  mass  by  some  eager  gold  seeker.  The  rock 
is  a fresh,  even  grained  aggregate  of  orthoclase  and  quartz.  Any  origi- 
nal micaceous  constituent  seems  to  be  lacking,  although  good-sized 
plates  of  muscovite  have  been  secondarily  developed  at  the  expense  of 
the  orthoclase.  This  feldspar  possesses  a beautiful  zonal  structure, 
which  is  brought  out  in  unusual  distinctness  by  the  different  degrees  to 
which  the  alteration  has  progressed  in  different  zones.  The  eruption  of 
this  rock  must  have  taken  place  subsequently  to  the  dynamic  move- 
ments which  metamorphosed  so  many  of  the  Marquette  intrusives.  It 
shows  no  evidence  of  pressure  in  its  microscopic  structure,  although 
No.  11658,  collected  but  a few  feet  north  of  it,  from  a narrow  baud  of 
acid  rock,  shows  such  evidence  in  a very  marked  degree. 

Quartz  porphyries.— No  rocks  are  better  suited  to  exhibit  the  effects 


WILLIAMS.  J 


QUARTZ  PORPHYRIES  AT  MARQUETTE. 


149 


of  dynamic  metamorphism  than  the  quartz  porphyries.  Some  of  the 
more  important  results  which  this  class  of  rocks  has  yielded  to  Euro- 
pean students  have  already  been  stated  in  Chapter  I.  Near  Marquette 
the  narrower  of  the  dikes  and  intrusions  of  granitic  matter  have,  in 
consequence  of  their  rapid  cooling,  assumed  this  form.  Almost  every 
variety  of  structure  between  a typical  granite  and  quartz  porphyry 
may  be  found  by  comparing  specimens  from  the  different  exposures. 
Furthermore,  the  various  dikes  seem  to  have  been  subjected  to  differ- 
ent degrees  of  mechanical  action,  so  that  the  successive  phases  of  meta- 
morphism may  be  traced  by  a comparative  study  of  them. 

In  No.  11629  we  have  a granitoid  porphyry  which  has  suffered  much 
from  chemical,  but  very  little  from  mechanical  alteration.  This  was 
collected  from  a branching  dike  of  a massive,  reddish  rock,  exposed  on 
the  lake  shore  near  the  water- works  in  Marquette.  It  approaches  a 
granite  in  being  largely  composed  of  porphyritie  feldspar  crystals  with 
but  comparatively  little  interstitial  groundmass.  What  there  is  of  this 
groundmass  consists  of  a fine  granular  mosaic  of  quartz  and  feldspar 
grains  with  some  sericite.  The  larger  feldspar  crystals  are  colored  red 
by  an  abundance  of  fine  globulitic  dust.  They  also  show  an  advanced 
stage  of  chemical  alteration  in  the  development  in  them  of  a micaceous 
mineral  (sericite).  The  only  traces  of  the  original  biotite  consist  of 
chlorite  areas  dotted  over  with  iron  hydroxide.  At  first  glance  this  rock 
seems  to  resemble  No.  11678  (above  described  as  a fine  example  of 
Tornebohm’s  mortar  structure),  but  a closer  examination  shows  that  the 
structures,  apparently  so  much  alike,  must  have  been  produced  by  very 
different  means.  There  is  in  the  present  instance  no  evidence  of  press- 
ure, the  feldspar  crystals  have  their  original  outlines  intact,  and  the  in- 
terstitial mosaic,  instead  of  being  due  to  a grinding  action  between  the 
grains,  is  here  evidently  a product  of  the  original  crystallization. 

The  next  specimen,  No.  11620,  is  a typical  quartz  porphyry  which  also 
has  been  but  little  modified  by  the  effects  of  pressure.  It  is  from  a 
small  dike  at  the  eastern  extremity  of  Lighthouse  Point  and  is  a much 
fresher  rock  than  the  last.  The  porphyritie  crystals  are  both  smaller 
and  less  frequent.  They  consist  of  oi  thoclase,  plagioclase,  and  quartz, 
imbedded  in  an  abundant  inicrogranitic  groundmass.  The  ortlioclase 
often  shows  a twinning  structure  in  accordance  with  the  Carlsbad  law 
and  is  extensively  altered  to  muscovite,  large  plates  of  which  occur 
around  its  crystals.  The  quartz  does  not  here  possess  its  characteristic 
dihcxahedral  form,  but  occupies  oval  or  irregularly  shaped  areas  which 
are  frequently  composite. 

These  two  specimens  will  serve  as  representatives  of  those  acid  dike- 
rocks  which  have  been  least  modified  by  pressure.  They  will  serve  as 
a starting  point  for  tracing  the  successive  stages  of  this  action  in  the 
following  specimens.  The  changes  observed  are : The  deformation  and 
elongation  of  the  quartz  crystals;  the  fracturing  and  separation  of  the 
fragments  of  feldspars;  the  parallel  arrangement  of  the  new  crystalliza- 


150 


GREENSTONE  SCHIST  AREAS  OF  MICHIGAN. 


[BULL.  62. 


tion products,  giving  rise  to  a gneissic  or  “flaser”  structure;  and  the 
development  of  a cleavage.  The  intensity  of  these  changes  is  of  course 
proportionate  to  the  amount  of  force  exerted. 

No.  11633,  obtained  from  the  quarry  on  Lighthouse  Point  (A  of  map, 
PI.  VII),  is  a quartz  porphyry  which  differs  ouly  slightly  from  No.  11620, 
last  described.  Its  groundmass  is  somewhat  finer  grained  and  sericitic. 
The  porphyritic  crystals  of  feldspar  are  nearly  the  same,  but  the  quartzes 
are  deformed  and  lenticular,  sometimes  with  only  an  undulatory  extinc- 
tion, sometimes  broken  into  several  areas  which  are  more  or  less  dis- 
placed from  their  original  position.  Although  the  thin  section  shows 
no  indications  of  schistose  structure,  this  in  the  field  is  quite  pronounced. 
The  rock  occurs  in  the  green  schist,  in  small  bands,  which  wedge  out 
very  soon.  It  has  a decided  tendency  to  break  along  planes  parallel  to 
the  schist-bedding,  and  upon  these  planes  of  parting  sericite  is  abun- 
dantly developed. 

No.  11653,  from  the  northern  edge  of  Lighthouse  Point,  just  below  the 
Lighthouse,  is  very  similar  to  the  last,  except  that  here  a schistose 
structure  is  microscopically,  as  well  as  macroseopically,  visible.  The 
groundmass  and  porphyritic  crystals  are  quite  identical  with  those 
above  described.  In  the  former  there  is  a brown  mica  abundantly  de- 
veloped in  aggregations  of  little  plates,  which  form  sinuous  lines  around 
the  porphyritic  crystals  in  a direction  parallel  to  the  strike  of  the  sur- 
rounding greenstone  schists.  This  fact  is  mentioned  by  Dr.  Wadsworth, 
who  was  the  first  to  discover  these  rocks.1 

Nos.  11707  and  11717,  were  collected  from  two  dikes  of  porphyry  inter- 
laminated  with  the  green  schists  of  the  Brook  section.  In  the  hand  speci- 
mens they  exhibit  no  marked  foliation,  but  under  the  microscope  their 
evidences  of  mechanical  alteration  are  most  interesting  and  instructive. 
The  groundmass  is  of  the  same  character  as  that  already  described. 
In  it,  however,  are  sinuous  bands  of  green  mica  which  bend  and  wind 
about  the  porphyritic  crystals  so  as  to  produce  a decided  u micro-flaser” 
structure.  This  feature  is  more  pronounced  in  the  second  specimen, 
although  the  two  are  essentially  the  same.  The  microscopic  appear- 
ance of  11707  is  represented  in  PI.  XV,  fig.  2.  The  porphyritic  feld- 
spars have  suffered  little  or  no  change,  unless  it  be  by  the  production 
of  microcline  which  is  quite  abundant  in  the  center  of  some  of  the  crys- 
tals of  No.  11707.  The  quartz  has  suffered  much  more  deformation — 
a fact  which  the  observations  of  J.  Lehmann2  and  Oh.  E.  Weiss3 
would  indicate  to  be  the  rule  in  rocks  of  this  character.  In  the  present 
case  the  quartz  is  drawn  out  into  long,  spindle  shaped  lenses  which  are 
often  pinched  at  their  ends  into  fine  lines  that  bend  around  the  other 
porphyritic  crystals  (see  PI.  XV,  fig.  2).  This  deformation,  however, 

•Notes  on  the  Iron  and  Copper  Rocks  of  Lake  Superior.  Bull.  Mus.  Comp.  Zool.,  Harvard  Coll. 
Whole  Series,  vol.  8,  Geol.  Series,  vol.  1,  p.  38. 

2Untersuchungon  ilber  die  Entstehung  der  altkrystallinischen  Schiefergesteine.  Bonn,  1884. 

3Zeitsehr.  Deutsch.  geol.  Gesell.,  vol.  29, 1877,  p.  418,  and  Jahrbuch  preuss.  geol.  Landesanstalt  fur 
1883,  p.  213.  Cf.  Rosen busch:  Mikros.  Physiog.,  2d  ed.,  vol  2, 1887,  p.  412. 


WILLIAMS.] 


TUFFS  OF  THE  QUARTZ  PORPHYRIES. 


151 


does  not  take  place  without  the  loss  of  continuity  in  the  quartz  sub- 
stance. On  the  contrary  a mosaic-like  aggregate  of  interlocking  grains 
is  formed  whose  optical  orientation  differs  more  and  more  in  proportion 
as  the  original  quartz  crystal  is  elongated.  In  cases  where  the  deforma, 
tion  is  slight,  only  a disturbed  extinction  results,  as  may  be  seen  in  Ho. 
11753.  The  presence  of  interlocking  grains  of  different  orientation,  as 
in  this  instance,  would  indicate  solution  and  subsequent  deposition. 

Ho.  11658,  from  a narrow  acid  band  immediately  north  of  the  granite 
boss  near  Pine  street,  Marquette,  is  a rock  of  precisely  the  same  type  as 
those  just  described  but  which  shows  a secondary  schistose  structure 
more  perfectly  developed  than  any  of  the  preceding.  The  brownish  or 
greenish  mica  is  here  arranged  in  nearly  parallel  bands  which  bend 
only  slightly  around  what  were  once  porphyritic  feldspar  crystals. 
These  latter  have  undergone  an  almost  complete  change  to  muscovite 
and  quartz  aggregates,  some  of  which  are  now  drawn  out  into  long  len- 
ticular areas.  These  patches  are  hardly  to  be  distinguished  from  the 
groundmass,  except  by  their  coarser  grain,  and  yet  they  can  be  traced 
with  certainty  back  to  the  original  orthoclase.  Sharp  crystals  of  pyrite 
and  some  epidote  are  also  developed  in  this  rock. 

Tuffs  of  the  acid  rocks. — Closely  allied  to  these  schistose  porphyries 
which  occur  in  dikes  are  certain  banded  acid  rocks  whose  most  impor- 
tant exposures  are  along  the  southern  edge  of  the  northern  Marquette 
greenstone  area,  near  the  junction  of  this  with  the  fissile  argillaceous 
shales  of  the  “ Eureka  series.”  These  are  hard,  compact,  fine  grained, 
but  decidedly  schistose  beds,  locally  known  as  novaculite.  Indeed, 
these  rocks  have  been  worked  to  a limited  extent  as  whetstone,  whence 
the  name  of  the  small  creek  flowing  through  the  southern  part  of  Mar- 
quette. 

The  color  of  these  so-called  novaculites  is  sometimes  reddish,  some- 
times pale  greenish  or  yellowish.  They  are  very  frequently  stiiped  with 
different  shades.  Under  the  microscope  they  closely  resemble  the 
groundmass  of  the  quartz  porphyries  described  in  the  last  section.  Ho 
porphyritic  crystals,  however,  are  ever  observed,  and  the  structure  is 
too  fine  grained  to  appear  schistose  in  a thin  section. 

Three  essentially  identical  sections  of  these  rocks  were  studied  from 
specimens  collected  at  three  of  the  most  typical  exposures. 

Ho.  11627  is  from  near  Burgess’s  saw-mill,  at  the  east  end  of  Lake 
street,  Marquette.  It  has  a reddish  color  produced  by  an  abundance  of 
iron  hydroxide  scales.  The  grain  is  for  the  most  part  quite  regular, 
although  larger  and  angular  quartz  fragments  are  occasionally  seen. 

Ho.  11684  was  taken  from  the  glaciated  exposure  of  the  novaculites, 
occurring  at  the  west  end  of  Ridge  street,  Marquette.  A fresh  fracture 
in  this  rock  shows  a light  gray  color.  It  is  parted  by  intersecting  joint 
systems  into  sharp  rhomboidal  prisms  which  strike  slightly  south  of 
west.  Under  the  microscope  this  rock  appears  as  a fine,  even  mixture 
of  quartz  grains  and  sericite  flakes. 


152 


GREENSTONE  SCHIST  AREAS  OF  MICHIGAN. 


[bull.  62. 


No.  11676  was  collected  at  the  south  end  of  the  “ Brook  section,” 
near  Steinbrecher’s  house.  (B  of  map,  Plate  VII.)  It  is  quite  similar 
to  the  others,  but  it  is  much  seamed  with  infiltrated  quartz,  small  veins 
of  which  appear  in  the  microscopic  section. 

The  regular  banding  of  these  anomalous  acid  rocks,  as  well  as  their 
interstratification  with  and  gradual  passage  into  the  similarly  banded 
greenstone  schists,  will  not  admit  of  the  supposition  that  they  wereever 
eruptive  masses,  however  much  we  may  imagine  these  to  have  been 
metamorphosed.  On  the  other  hand,  their  similarity,  in  both  composi- 
tion and  structure,  to  the  groundmass  of  the  quartz  porphyries,  is  too 
striking  to  be  overlooked. 

Apparently  only  two  hypotheses  are  altogether  reconcilable  with  the 
observed  facts : First,  that  the  rocks  are  true  sediments,  like  those  of 
the  Eureka  series,  along  whose  northern  edge  they  lie,  which  may  have 
been  largely  derived  from  disintegrated  quartz  porphyry  material ; or 
second,  that  they  are  consolidated  acid  tuifs  which  accompanied  the 
eruptions  of  the  porphyries,  in  the  same  manner  that  some  of  the 
greenstone  schists  represent  the  fragmental  diabase  material. 

Another  possible  supposition  is  that  these  compact,  hornstone-like 
rocks  resulted  from  the  contact-metamorphism  of  preexistent  sediments 
by  the  diabase  eruptions.  Such  an  effect  has  been  extensively  pro- 
duced by  the  Hartz  Mountain  diabase,  as  has  been  shown  by  the  work 
of  Lossen  and  others.  The  resultant  rock  is  known  as  adinole , but 
it  differs  essentially  from  the  Marquette  novaculite  in  a constant  and 
high  percentage  of  soda,  due  to  the  presence  of  albite.  This,  as  may 
be  seen  from  the  following  analysis,  is  absent  from  the  Marquette  rock. 
We  further  have  no  evidence  of  the  existence  of  sediments  when  the 
greenstones  were  produced,  as  all  the  Huronian  beds  are  younger. 

Of  the  two  first  mentioned  hypotheses,  the  second  is  the  more  proba- 
ble, first,  because  of  the  very  constant  character  of  these  banded  acid 
rocks,  and  second,  because  of  their  almost  exact  identity  in  chemical 
composition  with  the  massive  acid  eruptives.  The  following  chemical 
analysis  of  specimen  No.  11681,  from  the  west  end  of  Ridge  street,  Mar- 
quette, was  made  by  Mr.  W.  F.  Hillebrand  : 


Silica  (Si02) 

...  76.99 

Potash  (K20) , 

3. 65 

Alumina  (A1203) 

...  13.92 

Soda  (Na20) 

0. 56 

Ferric  oxide  (Fe203) 

0.45 

Lithia  (Li20) 

Trace. 

Ferrous  oxide  (Fe  0) 

0.77 

Water  (H20) 

2. 35 

Manganous  oxide  (MnO) 

Lime  (CaO) 

Magnesia  (MgO) 

...  Trace 

Phosphorous pentoxide  (P205)... 

Trace. 

Total 

100. 13 

It  will  be  seen  that  this  is  the  composition  of  an  aggregate  of  quartz 
and  sericite,  as  the  microscope  shows  our  novaculite  to  be.  The  sericite 
is  in  all  probability  the  result  of  the  alteration  of  original  orthoclase. 

The  occurrence  of  similar  tuff  deposits  in  connection  with  eruptive 
quartz  porphyries  is  well  known  in  Europe,  especially  in  the  German 


WILLIAMS.] 


ACID  TUFFS  FROM  OTHER  LOCALITES. 


153 


dyas.  They  have  been  carefully  studied  and  described  in  Saxony,1  the 
Yosges  Mountains,2  the  Black  Forest,3  and  Odenwald.4  The  writer  can 
speak  from  a very  considerable  personal  acquaintance  with  the  Black 
Forest  and  Odenwald  tuffs,  of  their  very  close  resemblance  to  the  Mar- 
quette novaculites. 

But  perhaps  the  closest  analogues  of  the  Marquette  tuffs  are  to  be 
found  among  those  described  by  Dr.  Archibald  Geikie,  from  St.  David’s, 
in  Wales,5  a region  which,  as  we  shall  see  in  the  sequel,  presents  many 
points  of  resemblance  to  the  Marquette  district.  The  analysis  of  one  of 
them,  hereafter  quoted  (Y),  agrees  very  closely  with  that  of  our  novac- 
ulite.  Dr.  Geikie  finds  that  these  acid  tuffs  accompanied  superficial 
eruptions  of  quartz  porphyries,  which  were  intimately  associated  with 
more  abundant  and  contemporaneous  extrusions  of  diabase  and  diabase 
tuffs.  The  acid  tuffs  have  been  derived  from  true  fine  grained  felsites. 
Some  of  them  are  conglomeratic  (agglomerates);  some  of  them  fine  ashy 
material,  which  has  become  consolidated  into  a sericitic  schist.  There 
are  various  intermediate  varieties  between  the  acid  and  basic  types, 
due  to  the  mingling  in  different  proportions  of  the  two  kinds  of  debris. 

Mr.  J.  S.  Diller6  has  also  shown  that  the  felsitic  rock  from  Breakheart 
Hill,  near  Saugus,  Massachusetts,  is  a silicified  quartz  porphyry  tuff; 
and  from  the  sharply  angular  shape  of  the  quartz  fragments,  of  which 
it  is  now  composed,  he  concludes  that  these  are  pseudomorphs  after 
fragments  of  an  acid  glass  originally  deposited  as  a volcanic  ash. 

The  following  analyses  of  well  characterized  acid  tuffs  from  European 
localities  are  here  quoted  on  account  of  their  similarity  to  the  Mar- 
quette novaculite : 


I. 

II. 

III. 

IV. 

V. 

Silica  (Si02)  

Alumina  (AI2O3) 

Ferric  oxide  (Fe203) > 

Ferrous  oxide  (FeO) > 

Lime  (CaO) 

76.  37 
13. 94 

3.18 

79. 73 
11.34 

0.99 

82. 47 
9.  55 
c 0.43 
l 0.57 
0.  53 
trace  . . . 
4.69 
0.58 
1.18 

84. 12 
9. 38 

| 1.78 

0.  08 
0.01 
0. 85 
0. 25 
3.  68 

80.59 
11.29 
r 0.28 

l *1. 41 
0.52 
0.95 
2.  98 
0. 72 
tl.96 

Magnesia  (MgO) 

Potash  (K20) 

Soda  (Na^O)  

Water  (H20) 

Total 

4.39 
1.07 
1.  58 

0.27 
3.81 
0. 17 
2. 12 

100. 53 

98. 43 

100. 00 

100. 15 

100. 70 

* Manganous  oxide  trace.  tLoss  on  ignition  and  water. 


1 C.  F.  Naumann:  Geognosie,  2d  ed.,  vol.  1,  p.  671,1858.  Also  Erlauterungon  zur  geol.  Specialkarte 
des  kon.  Sachsens,  Sect.  Frohburg  (59),  Colditz  (44),  Dobeln  (46),  Leisnig-Lausigk  (43),  and  Rochlitz 

(60). 

2D.  Gerhard : Geognistisch-petrographische  Mittheilungen  aus  dem  Gebweiler-Thal,  1880.  (Cf.  Noues 
. Jabrbucb  fur  Mineral.,  1881,  vol.  1,  Referate  p.  374). 

‘‘G.  H.  Williams:  Neues  Jahrbuch  fiir  Mineral.,  Boilage-Band  2,  pp.  626-634. 

4Benecke  and  Cohen  : Geogn.  Beschr.  d.  Umgegend  von  Heidelberg,  1881.  pp.  221-235. 

6 On  the  supposed  pre-Cambrian  rocks  of  St.  David’s.  Quart.  Jour.  Geol.  Soc.  London,  vol.  39,  pp. 
298-301, 1883. 

r,The  felsites  and  their  associated  rocks  north  of  Boston.  Proc.  Bost.  Soc.  Nat.  Hist.,  vol.  20,  pp. 
365-368;  Bull.  Mus.  Comp.  Zool.,  Harvard  Coll.  Whole  Series,  vol.  7,  pp.  165-180;  also  Science,  1884. 
vol.  3,  p.  653. 


154 


GREENSTONE  SCHIST  AREAS  OF  MICHIGAN. 


[BULL.  62. 


I.  Thonstein  (tuff)  from  Zeisigwald,  near  Chemnitz,  Saxony.1 

II.  Same.2 

III.  Silicified  tuff,  Oelberg,  near  Schriesheim,  Odenwald.3 

IV.  Silicified  tuff,  Kesselberg,  near  Triberg,  Black  Forest.4 

V.  Felsitic  tuff  breccia,  Clegyr  Hill,  St.  David’s,  Wales.5 

If,  then,  these  banded  acid  rocks  occurring  near  Marquette,  as  seems 
most  probable,  really  do  represent  solidified,  tuff  material  of  the  quartz 
porphyries,  we  might  expect  to  find  transitional  forms,  grading  into  the 
banded  green  schists.  These  do  appear  to  exist,  and  indicate  that 
some,  at  least,  of  the  eruptions  of  both  acid  and  basic  rocks  were  nearly 
contemporaneous. 

BANDED  GREENSTONE  SCHISTS. 

The  banded  greenstone  schists  which  form  the  prevailing  rock  over  the 
northern  portion  of  the  Marquette  area  have  been  regarded  by  all  geolo- 
gists who  have  ever  studied  them  as  originally  sedimentary  deposits, 
and  a repeated  examination  of  them  in  the  field  seems  incapable  of 
leading  to  any  other  conclusion.  They  are  everywhere  stratified  with 
the  greatest  regularity  in  bands  of  lighter  and  darker  shades  of  green. 
This  structure  is  to  be  most  advantageously  seen  in  the  woods  just 
north  of  Marquette  and  near  Lighthouse  Point.  Here  glaciated  areas 
of  considerable  extent  often  show  a finely  ribboned  appearance,  looking 
as  though  the  sharp,  parallel  lines  had  been  drawn  with  a ruler.  The 
alternation  in  the  color  and  composition  of  the  layers  is  so  frequent  and 
so  constant,  and  their  parallelism  to  the  east  and  west  strike  of  all  the 
rocks  of  this  neighborhood  is  so  exact  that  no  hypothesis  of  their  orig- 
inally massive  character  will  satisfactorily  account  for  the  observed 
facts. 

On  the  other  hand,  the  chemical  and  the  microscopical  characters  of 
these  schists  agree  closely  with  those  of  associated  massive  greenstones 
which  are  known  to  have  been  derived  by  the  alteration  of  basic  erup- 
tive rocks.  Both  are  composed  of  fibrous  green  hornblende,  quartz, 
epidote,  zoisite,  and  chlorite.  There  must,  therefore,  have  been  a close 
similarity  in  the  original  composition  of  these  two  classes  of  rocks,  in 
spite  of  the  wide  difference  in  their  structure. 

Prof.  M.  E.  Wadsworth,  who  has  ably  advocated  the  eruptive  origin 
of  many  of  the  rocks  occurring  near  Marquette,  regards  these  banded 
schists  as  undoubtedly  of  sedimentary  origin.  He  says:6 

The  schist  from  the  same  specimen  (45)  is  composed  of  quartz,  argillaceous  mate- 
rial, chlorite,  hornblende,  magnetite,  “ leucoxene,”  and  a little  augite.  It  would  seem 
that  this  had  been  formed  from  detrital  material  of  the  same  nature  as  the  dikes 
(basaltic).  The  close  resemblance  of  the  “diorite”  and  schist  in  mineralogical  char- 
acters, but  not  in  structure,  is  shown  in  another  section  containing  the  junction  of  the 
two  rocks  (48).  ^ . 

1 Neues  Jahrbneh  fur  Mineral.,  1864. 

2 Ibid.,  1859. 

3 Die  zur  Dyas  gehcirigen  Gesteino  des  siidlichon  Odenwaldes,  von  E.  Cohen,  1871,  p.  57. 

* Neues  Jahrbuch  fur  Mineral.,  Beilage-Band  2,  p.  630. 

8 Quart.  Jour.  Geol.  Soc.  London,  vol.  39,  1883,  p.  297. 

6Notos  on  the  Iron  and  Copper  Districts  of  Lake  Superior.  Bull.  Mus.  Comp.  Zool.,  Harvard  Coll., 
Whole  Series,  vol.  7,  Geol.  Series,  vol.  1,  p.  37. 


Williams. J SHEAF-LIKE  HORNBLENDE  IN  THE  BASIC  TUFFS.  155 

Specimes  of  these  banded  greenstone  schists  which  were  collected 
from  different  localities  within  the  northern  Marquette  area,  although 
they  are  macroscopically  nearly  identical,  present  a great  variety  in 
their  microscopical  structure. 

Nos.  11618  and  11619,  from  Lighthouse  Point,  Marquette,  are  com- 
paratively coarse  grained  rocks  composed  largely  of  a green  fibrous 
hornblende.  The  structure  of  this  mineral,  especially  in  No.  11619,  is 
unusual.  What  at  first  glance  looks  like  a confused  mass  of  irregular 
and  ragged  hornblende  areas,  when  more  carefully  examined,  is  found 
to  consist  of  more  or  less  radiating  bundles  of  hornblende  fibers,  resem- 
bling sheaves.  The  center  of  these  bundles  is  their  most  compact  por- 
tion. Here  the  hornblende  substance  is  often  continuous  and  homo- 
geneous, but  toward  the  two  ends  of  the  mass  it  appears  to  be  frayed 
out  into  separate  fibers.  These  are  so  regularly  divergent  in  their  ar- 
rangement as  to  produce  a black  brush  which  sweeps  across  them  as 
the  stage  of  the  microscope  is  revolved  between  crossed  Nicol  prisms. 
This  peculiar,  sheaf-like  grouping  of  the  hornblende  is  shown  in  PI.  XVI, 
Fig.  1.  It  is  very  similar  to  that  described  by  de  la  Vallee-Poussin  and 
Renard  in  an  amphibolite  occurring  near  Laifour,  in  the  valley  of  the 
Meuse,1  and  by  Renard  in  the  metamorphosed  Devonian  slates  of  Bas- 
togne  in  the  Ardennes  Mountains.2  Though  it  can  still  be  traced  in 
specimen  No.  11618,  this  structure  is  by  no  means  as  distinct  as  in  the 
case  just  described. 

The  groundmass  in  which  this  hornblende  lies  is  a finely  granular 
aggregate  of  albite,  or  quartz  and  albite  grains.  In  it  occur  some 
chlorite,  epidote,  or  zoisite  in  good  sized  individuals,  and,  at  least  in 
No.  11619,  some  small  ilmenite  particles,  surrounded  by  a highly  refrac- 
tive leucoxene  border.  There  is  comparatively  little  groundmass  in 
either  of  these  specimens,  but  of  the  two  No.  11618  contains  the  more. 

Nos.  11730,  from  the  western  part  of  Marquette,  between  Michigan 
and  Ohio  streets,  and  11734,  from  the  corner  of  Front  and  Ohio  streets, 
are  both  banded  greenstones  of  the  same  type  as  the  specimens  last 
described.  The  former  contains  less  hornblende,  though  this  mineral, 
is,  nevertheless,  abundant  in  the  same  sheaf  like  bundles  as  before. 
The  groundmass  is  a fine  grained  albite  mosaic,  which  contains  some 
quartz  and  some  epidote.  The  latter  specimen,  No.  11734,  is  largely 
composed  of  an  unusually  dark  green  and  pleochroic  hornblende,  in  con- 
fused ragged  and  fibrous  groups.  Along  certain  lines,  where  this  compo- 
nent is  less  abundant,  the  rock  assumes  a lighter  shade.  The  albite  mo- 
saic is  present,  but  not  to  the  exclusion  of  areas  of  gray  saussurite, 
which  sometimes  show  indications  of  a latli-like  form,  like  that  of  the 
diabase  feldspars.  Narrow  seams  filled  with  epidote,  or  an  aggregate 
of  albite  and  epidote,  traverse  this  rock  parallel  to  its  banding.  Ilmen- 
ite grains,  with  their  rims  of  leucoxene,  occur  in  each  of  these  specimens. 

*M6m.  sur  les  char.  min.  et  strat.  des  roches  dites  plutoniennes,  etc.,  Brussels,  1876,  p.  252,  PI.  V, 

Fig.  25. 

2 Les  roches  gr6natif6res  et  amphiboliques  do  la  r6gion  de  Baatogno.  Bull.  Mus.  roy.  d’liist.  nat.  de 
Belgique,  1882. 


156  GREENSTONE  SCHIST  AREAS  OF  MICHIGAN.  [bull.  62. 

There  is  nothing  in  the  microscopical  structure  of  these  slides  to  sug- 
gest a massive  eruptive  rock;  on  the  contrary,  the  two  instances  cited, 
where  a similar  sheaf  like  hornblende  has  before  been  noticed,  are  cases 
of  supposed  metamorphosed  tuffs. 

No.  11630,  from  the  quarry  on  Lighthouse  Point  (A  of  map,  PI.  YII)  is 
also  largely  composed  of  hornblende  in  pale  green,  ragged-looking  indi- 
viduals, but  without  any  of  the  sheaf-like  structure.  Amid  the  horn- 
blende a clear  transparent  feldspar,  evidently  albite,  has  been  abund- 
antly developed  in  good-sized  grains,  which  show  a sharp  twinning  stri- 
ation.  The  gradation  of  this  well  characterized  albite  into  the  granu- 
lar mosaic  lends  additional  force  to  the  supposition  that  this  also  is  com- 
posed of  the  same  mineral,  as,  indeed,  Lossen  has  shown  to  be  the  case 
in  many  of  the  regionally  metamorphosed  diabases  of  the  eastern  Hartz.1 

Nos.  11631  and  11637  are  other  specimens  of  the  banded  greenstone 
schists  from  the  same  quarry  as  the  last  on  Lighthouse  Point.  The  for- 
mer is,  perhaps,  the  most  typical,  although  an  abundance  of  calcite 
shows  that  it  is  mueh  weathered.  Its  alternating  light  and  dark  green 
bands  are  due  to  the  fact  that  hornblende  is  still  present  in  the  latter, 
while  its  place  is  supplied  in  the  lighter  colored  bands  by  a pale  chlor- 
ite and  epidote.  An  opaque  iron  oxide,  often  surrounded  by  a leu- 
coxene  rim,  is  found  in  small  particles  scattered  through  this  rock,  as 
is  also  a little  biotite.  The  second  of.  the  above  mentioned  specimens, 
Np.  11637,  which  was  taken  from  just  beside  the  great  dike,  shows  what 
the  last  described  rock  was  when  it  was  in  a fresher  condition.  The  cal- 
cite is  here  absent,  and  the  rock  is,  for  the  most  part,  a mass  of  ragged 
and  raveled  hornblende.  Among  this  is  scattered  some  clear,  trans- 
parent feldspar  (probably  albite)  and  zoisite,  or  epidote,  which  occurs  in 
irregular  crystalloids,  arranged  in  long,  parallel  lines.  The  iron  mineral 
and  biotite  are  present  as  before. 

No.  11623,  found  beside  the  great  dike  on  Lighthouse  Point,  is  only 
a confused  aggregate  of  very  pale  and  very  fibrous  hornblende  needles 
with  calcite.  Lighter  bands  are  occasioned  in  this  rock  by  a prepon- 
derance of  calcite  and  chlorite  over  the  hornblende. 

No.  11626  is  a gray  schistose  rock  from  the  exposure  near  Burgess’s 
saw  mill,  on  Lake  street,  Marquette.  It  is  full  of  calcite,  which  is  ar- 
ranged in  bands  along  with  a very  finely  granular  mosaic.  Hardly  any 
hornblende  is  visible  in  this  specimen,  but  veins  of  epidote  and  some 
chlorite  occur  in  it. 

Along  the  deep  north  and  south  exposure  of  the  greenstone  schists 
which  has  been  described  as  the  Brook  section,  these  banded  greenstones 
• are  also  very  admirably  displayed.  For  the  most  part  they  are  qtfite 
like  those  occurring  in  the  neighborhood  of  Marquette.  In  one  par- 
ticular, however,  some  of  them  present  an  unusual  feature  which  it  is 
not  altogether  easy  to  explain.  This  consists  in  the  presence  of  len- 

1 Zeitscbr.  Deutsch.  pool.  GeselJ.,  vol.  24,  1872,  p.  730.  Jahrbucli  preuss.  geol.  Landesanstalt  fur 
1883,  p.  640;  ibid.,  fiir  1884,  p.  528.  Eriaut.  zur  geol.  Specialkarte  von  Pr.,  Blatt  Wippra,  Berlin,  1883. 


WILLIAMS.]  WHITE  AUGEN  IN  THE  GREENSTONE  SCHISTS.  157 

ticular  masses  of  a white  feldspathic  substance,  which  are  so  elongated 
in  the  direction  of  the  bedding  that  while  they  generally  present  a 
lens-shaped  form,  their  cross-section  is  nearly  circular.  The  size  of 
these  lenses,  which  externally  resemble  what  the  Germans  call  “Augen” 
or  eyes,  is  extremely  variable.  Some  are  smaller  than  peas,  while  others 
are  more  than  two  inches  in  length.  The  extent  also  to  which  they  are 
elongated  differs  very  much  in  different  cases.  Some  are  represented 
only  by  narrow  white  lines  which  are  occasionally  thickened  or  swelled 
out  into  oval  spots.  Between  these  and  such  as  vary  comparatively 
little  from  a spherical  form  we  may  find  all  intermediate  stages. 

These  white  lenses  are  by  no  means  universally  distributed  through 
the  green-schists  of  the  Brook  section;  on  the  contrary  they  occur  only 
rarely  in  bands  which  transverse  the  greenstones  parallel  to  their  bed- 
ding. One  of  these  bands  consisted  of  only  a few  rows  of  large,  oval 
masses,  exactly  resembling  rounded  pebbles,  but  in  spite  of  its  narrow- 
ness it  could  be  traced  for  a considerable  distance. 

The  white  color  of  these  lenses  or  “Augen”  presents  a decided  con- 
trast to  the  dark  green  of  the  inclosing  schists.  Their  outline,  too,  is 
quite  sharp,  and  yet,  upon  a close  examination,  they  are  seen  to  pass 
gradually  into  the  substance  of  the  surrounding  rock.  What  their 
origin  was,  whether  they  were  inclusions  much  flattened  by  subsequent 
pressure,  or  secretions  of  the  rock  itself,  or  infiltrations,  it  now  seems 
difficult,  if  not  impossible,  to  decide. 

Sections  11703  to  11705a,  show  the  microscopic  composition  and 
structure  of  these  lenticular  masses  as  well  as  their  relation  to  the  in- 
closing rock.  This  latter  is  in  all  cases  a typical  hornblende  schist  or 
amphibolite.  It  is  composed  of  small,  compact  needles  of  strongly 
pleochroic,  green  hornblende,  colorless  grains  of  feldspar  and  probably 
quartz,  and  the  minute,  highly  refractive  epidote  particles  so  character- 
istic of  the  crystalline  schists.  The  feldspar  is  very  fresh  and  free  from 
inclusions,  as  though  it  were  the  product  of  a new  crystallization.  It 
rarely  possesses  an  albite  or  microcline  twinning  structure,  but  for  the 
most  part  it  is  so  homogeneous  and  limpid  that  it  closely  resembles 
quartz.  Lossen  has  called  particular  attention  to  the  difficulty  of  dis- 
tinguishing a mosaic  of  secondary  albite  from  quartz  under  the  micro- 
scope,1 and  it  is  very  possible  that  quartz  grains  are  actually  present 
in  this  rock,  although  in  certain  favorable  cases  a biaxial  character  was 
substantiated. 

No.  11703  is  cut  in  the  direction  of  the  bedding  and  shows  the  horn- 
blende in  strictly  parallel  arrangement.  Its  feldspar  “Augen”  are  very 
much  elongated,  while  in  No.  11705,  which  is  cut  nearly  perpendicular 
to  the  bedding,  they  are  as  broad  as  they  are  long.  This  substance 
was  undoubtedly  once  some  triclinic  feldspar,  but  this  has  been  changed 
to  saussurite  which  now  consists  of  epidote  and  sericite  imbedded  in  a 


1 Zeitschr.  Deutscli.  geol.  Gesell.,  vol.  31,  1879,  p.  441,  et  seq.  Jahrbuch  preuss.  geol.  Landcsanstalt 
fur  1884,  pp.  528,  o44,  PI.  XXIX,  fig.  4. 


158 


GREENSTONE  SCHIST  AREAS  OF  MICHIGAN. 


IBULL.  62. 


new  crystallization  of  albite.  They  contain  no  hornblende,  but  there 
seems  to  be  a condensation  of  this  mineral  in  the  schist  around  their 
edge  and  enough  of  it  penetrates  for  a distance  into  their  substance  to 
form  a gradual  transition  rather  than  a sharp  line  of  contact  between 
them  and  the  inclosing  rock. 

The  composition  of  these  aAugen”  is  not  in  every  instance  the  same, 
although  they  all  appear  to  have  been  derived  from  some  form  of 
feldspar.  In  No.  11704  they  are  composed  wholly  of  epidote,  while  in 
No.  11705a  the  original  feldspar  was  more  acid  and  sericite  has  been 
produced  almost  to  the  exclusion  of  epidote. 

Other  of  the  banded  greenstones  collected  along  the  Brook  section 
are  quite  devoid  of  the  white  “Augen”  and  agree  closely  with  the  rocks 
around  Marquette. 

Nos.  11706,  11713,  and  11718  are  essentially  hornblende  rocks,  con- 
taining some  altered  feldspar  and  some  quartz.  They  are  plainly 
banded,  the  alternate  layers  differing  in  both  color  and  composition. 

No.  11671,  from  an  exposure  very  near  the  center  of  section  17,  con- 
sists of  sharp  epidote  needles  and  a little  quartz,  imbedded  in  a con- 
fused mass  of  pale  green,  fibrous  hornblende. 

Nos.  11610,  11611,  and  11667,  from  near  the  powder  mill  on  Dead 
Biver,  are  all  schistose  greenstones  in  a much  altered  condition  consist- 
ing now  of  chlorite,  quartz,  and  carbonates. 

As  has  been  already  remarked,  the  structure  of  these  greenstone- 
schists  is  such  as  to  necessitate  a belief  in  the  original  nature  of  their 
stratification;  while,  on  the  other  hand,  their  chemical  as  well  as  their 
mineralogical  composition  renders  it  impossible  to  separate  them  from 
the  massive  and  highly  altered  greenstones  (uralite  diabases,  etc.), 
with  which  they  are  most  intimately  associated.  Their  parallel  band- 
ing indicates  a fragmental,  but  their  chemical  and  their  mineral  com- 
position indicate  an  igneous  origin.  The  only  satisfactory  reconciliation 
of  these  opposite  sets  of  characters  is  to  be  found  in  that  group  of 
rocks  intermediate  between  sediments  and  lavas,  known  as  volcanic 
tuffs. 

In  the  opinion  of  the  writer,  then,  the  banded  greenstone  schists  of 
the  northern  Marquette  area  are  to  be  regarded  as  consolidated  and 
highly  metamorphosed  diabase  tuffs.  These  are  intimately  associated 
with  numerous  contemporaneous  flows  of  diabase  and  quartz  porphyry, 
together  with  tuffs  of  the  latter  rock ; while  all  have  been  broken  through 
by  much  younger  dikes,  both  basic  and  acidic. 

From  the  preceding  petrographical  descriptions  it  will  be  seen  how 
great  is  the  similarity  between  the  banded  greenstones  of  Marquette 
and  the  older  massive  diabases.  Mineralogically,  they  are  now  iden- 
tical, but  the  flue  parallel  banding  of  the  former  necessitates  the 
assumption  that  their  origin  differed  from  that  of  the  eruptives. 

In  a former  paper1  the  writer  has  maintained  that  two  geological 

1 Bull.  U.  S.  Geol.  Smvey,  No.  28,  p.  1. 


WILLIAMS.] 


ORIGIN  OF  THE  BANDED  GREENSTONES. 


159 


masses  as  different  in  tlieir  structure  and  origin  as  a clay-bank  and  a 
lava-stream,  if  they  possessed  the  same  chemical  composition  to  start  with , 
when  subjected  for  a long  period  to  exactly  the  same  physical  condi- 
tions, would  result  in  the  same  products.  This  is,  of  course,  true  only 
when  these  conditions  allow  of  profound  metasomatic  and  structural 
changes.  On  the  other  hand,  when  we  find  two  intimately  associated 
rocks  which  for  a long  time  have  been  subjected  to  exactly  the  same 
conditions,  but  which  still  bear  evidence  of  dissimilar  origin,  in  spite  of 
practical  identity  of  mineral  and  chemical  composition,  we  may  safely 
consider  them  as  originally  of  the  same,  or  of  similar  chemical  composi- 
tion. Now,  it  is  difficult  to  imagine  any  stratified  sediments  of  the 
composition  of  diabase,  except  diabase  ashes  j nor  could  these  have  un- 
dergone transportation  by  water  without  suffering  important  chemical 
changes.  We  therefore  conclude  that  the  banded  schists  represent  vol- 
canic debris  deposited  at  or  near  the  point  of  its  origin. 

In  order  to  obtain  a clear  idea  of  just  how  these  ancient  and  much 
disguised  tuffs  acquired  their  present  form  and  apparently  dual  char- 
acter, it  will  be  advantageous  to  ascertain  what  is  known  of  analagous 
formations  of  comparatively  recent  date.  Capt.  C.  E.  Dutton’s  de- 
scriptions1 of  the  fragmental  rocks  accompanying  the  Tertiary  erup- 
tives  of  the  high  plateaus  of  Utah,  are  well  suited  to  this  purpose.  He 
says,  in  speaking  of  the  extent  of  these  deposits  :2 

Some  of  the  most  interesting  lithological  problems  presented  by  the  volcanic  prod- 
ucts of  the  high  plateaus  are  those  relating  to  the  origin  and  development  of  what 
may  be  termed  the  clastic  igneous  rocks,  or  rocks  apparently  composed  of  fragmental 
materials  of  igneous  or  volcanic  origin,  but  now  stratified  either  as  so-called  tufa- 
ceous  deposits  or  as  conglomerates.  These  are  exceedingly  abundant  in  all  of  the 
great  volcanic  districts  of  the  world,  and  often  enormously  voluminous.  How  those 
of  the  high  plateaus  would  compare,  in  respect  to  magnitude,  with  those  of  other 
regions,  I do  not  accurately  know,  but  absolutely  their  bulk  is  a source  of  utter  aston- 
ishment. They  cover  nearly  2,000  square  miles  of  area,  and  their  thickness  ranges 
from  a few  hundred  feet  to  nearly  2,500  feet,  the  average  being  probably  more  than 
1,200  feet.  Lavas  are  frequently  intercalated,  but  much  more  frequently  no  inter- 
calary lavas  are  seen,  and  in  general  they  seldom  for  any  large  proportion  of  the 
entire  bulk  when  they  occur  in  conjunction  with  the  clastic  masses. 

Again,  in  speaking  of  the  peculiar  liability  of  such  deposits  to  meta- 
morphism, the  same  writer  says:3 

A very  striking  characteristic  of  these  clastic  volcanic  rocks,  both  the  tufas  and 
the  conglomerates,  is  their  great  susceptibility  to  raetamorphism.  Not  oulv  have  the 
beds  in  many  localities  been  thoroughly  consolidated,  but  they  have  undergone  crys- 
tallization. Those  tufas  and  conglomerates  which  are  of  older  date,  and  which  have 
been  buried  beneath  more  recent  accumulations  to  considerable  depths,  rarely  fail  to 
show  conspicuous  traces  of  alteration,  and  in  many  cases  have  been  so  profoundly 
modified  that  for  a considerable  time  there  was  doubt  as  to  their  true  character.  The 
general  tendency  of  this  process  is  to  convert  the  fragmental  strata  into  rocks  having 
a petrographic  facies  and  texture  very  closely  resembling  certain  groups  of  igneous 
rocks.  When  we  examine  the  rocks  in  situ  no  doubt  can  exist  for  a moment  that 


1 Report  on  the  Geology  of  the  High  Plateaus  of  Utah.  By  C.  E.  Dutton  ; Washington,  1880. 

* Ibid.,  p.  69.  3 ibid.,  pp.  79,  80. 


160 


GREENSTONE  SCHIST  AREAS  OF  MICHIGAN. 


[BULL.  62. 


they  are  water-laid  strata.  The  hand-specimens  taken  from  the  beds,  which  are  ex- 
tremely metamorphosed,  might  readily  pass,  even  upon  close  inspection,  for  pieces 
of  massive  eruptive  rocks  were  it  not  that  the  original  fragments  are  still  distinguish- 
able, partly  by  slight  differences  of  color,  partly  by  slight  differences  in  the  degree 
of  coarseness  of  texture.  But  the  matrix  has  become  very  similar  to  the  included 
fragments,  holding  the  same  kinds  of  crystals,  and  under  the  microscope  it  shows 
a groundmass  of  the  same  texture  and  composition.  # * * 

I see  nothing  at  all  incredible  in  the  idea  of  metamorphism  producing  rocks  so 
closely  resembling  some  eruptive  rocks  that  they  can  not  be  petrographically  distin- 
guished from  them.  It  seems  rather  that  we  ought  to  anticipate  just  such  a result 
from  the  alteration  and  consolidation  of  pyroclastic  strata.  The  materials  which 
compose  them  consisted  originally  of  disintegrated  feldspar,  pyroxene,  and  the  mat- 
ter which  constitutes  the  amorphous  base  of  all  eruptive  rocks. 

We  are  thus  enabled  to  see  that  there  is,  at  least,  no  geological  diffi- 
culty in  the  explanation  here  offered  of  the  origin  and  nature  of  the 
banded  green-schists  at  Marquette.  On  the  high  plateaus  of  Utah, 
which  form  one  of  many  similar  districts,  conditions  are  plainly  seen 
to  have  prevailed  quite  similar  to  those  here  assumed  for  the  more 
ancient  rocks  of  Lake  Superior ; and  yet  the  metamorphism  which  has 
taken  place  in  the  ancient  Archean  deposits  is  hardly  greater  than 
that  described  by  Captain  Dutton  in  the  tertiary  tuffs. 

The  most  generally  accepted  type  of  diabase  tuffs  is  the  German 
“ Schalstein  f but,  as  Rosenbusch  well  remarks,1  in  the  course  of  many 
years  so  many  totally  different  rocks,  with  only  the  most  superficial  re- 
semblance to  each  other,  have  been  described  under  this  designation, 
that  there  is  now  no  definite  meaning  whatever  which  can  be  attached 
to  this  term.  The  schalsteins  are  for  the  most  part,  green  or  greenish 
in  color,  earthy  and  schistose $ but  among  them  have  been  included 
altered  and  foliated  diabases  on  the  one  hand,  and  true  sediments  on 
the  other,  while  some  of  them  are  undoubtedly  true  diabase  tuffs.  In 
Germany  their  distribution  is  very  wide  in  Nassau,  Saxony,  and  Ba- 
varia. 

The  microscopic  sections  of  German  Schalsteins  accessible  to  me  for 
comparison  were  those  in  the  Stiirtz  collection  of  typical  rocks  belong- 
ing to  the  petrographical  laboratory  of  the  Johns  Hopkins  University. 
They  are  from  the  localities  of  Riibeland  in  the  Hartz  Mountains,  and 
Diez,  Baldinnstein,  Dillenburg,  and  Weilburg  in  Nassau.  In  spite  of 
extreme  alteration,  resulting  in  several  cases  in  the  survival  of  only 
chlorite,  calcite,  and  iron  oxide,  it  can  be  distinctly  seen  that  the  speci- 
mens were  originally  totally  different.  The  rocks  from  Diez,  Dillen- 
burg, and  two  out  of  the  three  labeled  Weilburg,  are  only  very  arnyg- 
daloidal  diabcses.  The  structure  in  the  base  is  well  preserved,  while 
the  amygdules  are  filled  with  calcite  surrounded  by  a rim  of  chlorite. 
The  rock  from  Riibeland  is  apparently  of  the  same  nature,  but  the  origi- 
nal structure  has  now  disappeared.  In  the  specimen  from  Baldinnstein 
and  m one  from  Weilburg  there  is  no  indication  of  diabase  structure, 
but  there  is  a spheroidal  aggregation  resembling  that  seen  in  palagonite. 


1 Mikros.  Physiog. , 2d  ed.,  vol.  2,  p.  245. 


WILLIAMS.] 


FOREIGN  DIABASE  TUFFS. 


161 


The  most  extended  descriptions  of  these  rocks  have  been  given  by  Gum- 
bel,  who  has  treated  the  schalsteins  of  the  Fichtelgebirge  in  Bavaria  in  a 
most  careful  manner.1  Rothpletz  has  described  the  tuffs  and  agglom- 
erates associated  with  the  Silurian  diabases  in  Saxony.2  In  Great 
Britain  the  ancient  volcanic  areas  of  Cornwall  and  St.  David’s  in  Wales 
show  the  closest  similarity,  both  in  the  character  of  their  rocks  and  in 
certain  features  of  their  structure  to  the  Marquette  region.  The  slaty 
blue  u eivans  ” of  the  former  district  were  regarded  by  De  la  Beche  as 
altered  ash-beds.3  J.  Arthur  Phillips  arrived  at  the  same  conclusion.4 
He  says : 

The  Coruish  rocks  afford  numerous  examples  of  ancient  lava  flows  so  interbedded 
with  slates  and  schists  of  the  district  as  to  lead  irresistibly  to  the  conclusion  that 
they  are  contemporaneous  ingeous  deposits. 

Also  again : 5 

The  slaty  blue  eivans  found  between  St.  Erth  and  St.  Stephens  (in  Bramwell)  have 
a chemical  composition  identical  with  that  of  the  altered  dolerites,  and  may  be,  as 
was  formerly  suggested,  highly  metamorphosed  ash-beds. 

The  basic  tuffs,  like  the  acid  ones,  occurring  at  St.  David’s  have  been 
described  by  Dr.  A.  Geikie.6  He  finds  that  all  varieties  of  texture  can 
be  traced,  from  large  grained  breccias  to  fine  schistose  mudstones.  The 
finer  material  includes  angular,  subangular,  and  rounded  blocks  or 
lapilli,  consisting  not  alone  of  diabase,  but  also  of  the  more  acid  felsitic 
rocks.  These  are  true  agglomerates,  and  their  striking  resemblance  to 
certain  other  of  the  schistose  greenstones  of  the  Marquette  belt  will 
be  alluded  to  in  the  sequel. 

• The  eruptive  rocks  which  Dr.  Hans  Beusch  has  recently  studied  in 
the  regionally  or  dynamically  metamorphosed  district  on  the  west  coast 
of  Norway,  present  a close  resemblance  to  those  occurring  near  Mar- 
quette.7 He  finds  diorites,  in  part  very  schistose,  which  have  originated 
through  the  metamorphism  (uralitization  and  epidotization)  of  ancient 

1 Geognostisclie  Beschreibung  ties  Fichtelgebirges,  mit  dem  Frankenwald  und  dem  westliclien  Vor- 
lande,  Gotha,  1879,  pp.  222  et  seq. 

2 Erl.  zurgeol.  Specialk.  Sachsens,  Sect.  Frankenberg-Hainichen(78),  j>p.  16  and  21 ; Sect.  Sekellenberg- 
Floka  (97),  p.  G». 

3 Geological  Observer. 

4 Quart.  Jour.  Geol.  Soc.  London,  vol.  34,  p.  493. 

5 Ibid,  p.  495. 

6 Quart.  Jour.  Geol.  Soc.  London,  vol.  39,  p . 297, 1883. 

7Geologische  Beobachtungen  in  einem  regional-metamorphosirten  Gebiet  am  Hardangorfjord  in 
Xorwegen,  Neues  Janrbuchfiir  Mineral.,  Beilage-Band  5,  pp.  52-67.  On  pages 54,  55  the  author  says: 
Nicht  selten  zeigt  das  dioritische  Gestein  einen  schichtenweisen  Weehsel  von  verschiedonen  Varie- 
taten.  In  diesem  Falle  bin  ich  geneigt,  anzunehmeu,  dass  das  urspriingliche  Gestein  nach  Art  der 
Tuffegebildet  wurde.  Dies  geschichtete  dioritische  Gestein  bildet  einen  Uebergang  zuden  griinlickeu 
feinkbrnigen  oder  dichten,  geschichteten,  mehr  oder  weniger  schieferigen  Gesteinsarten,  wolclie  die 
Hauptmasso  von  dem  ausmachen,  was  ich  fur  basische  Tuffe  halte.  Diese  Gesteine  fiihren  ala  woscnt- 
licho  Bestandtheilo  Hornblende,  Chlorit  und  Epidot,  daueben  gem  roichlich  Carbonspath.  Sie  ent- 
sprechen  eiuigermassen  den  Schalsteinen  der  deutschen  Petrographen.  Eingelagert  kommen  Masson 
vor,  die  man  am  ehesteu  fiir  geflossene  Strbmo  lialten  muss.  Einige  Bind  wohl  auch  intrusive  Gaugo. 
Uebrigens  ist  es  hier,  wie  anderswo  unter  ahnlichen  Verhiiltnissen,  oft  schwierig  zu  untorscheiden 
was  massig  erstarrtund  was  klastischo  Bildung  ist.  For  the  detailed  descriptions  of  these  rocks  by 
Dr.  Reusch,  see  “Bommelben  og  Karmben,”  Christiania,  1888  (in  Danish),  p.  112,  and  the  appended 
‘ English  summary  of  contents,  p.  402. 

Bull  Gli 11 


|M|M 


162 


GREENSTONE  SCHIST  AREAS  OP  MICHIGAN. 


[BULL  62. 


gabbros.  These  are  most  intimately  associated  with  granites  and  quartz 
porphyries,  while  both  acid  and  basic  rocks  are  accompanied  by  abun- 
dant tuff  deposits. 

In  America  hardly  anything  reliable  has  been  published  on  basic  tuffs. 
Edward  Hitchcock  speaks  of  diabase  tuffs  in  the  trias  of  Massachu- 
setts, but  gives  nothing  specific  respecting  their  nature.1  References 
to  this  class  of  deposits  are  scattered  through  the  writings  of  some  of 
the  Canadian  geologists,  especially  in  the  recent  report  of  Mr.  A.  C. 
Lawson  on  the  Lake  of  the  Woods  region.2 

1 Geology  of  Massachusetts,  4°,  1841,  p.  648. 

2 Geol.  and  Nat.  Hist.  Survey  Canada,  Ann.  Kept,  for  1885,  Kept.  CC.,  1886. 


. 


GREENSTONE  BELTS  OF  THE  MARQUETTE  DISTRICT— Continued. 

ROCKS  OF  THE  SOUTHERN  PORTION  OF  THE  MARQUETTE  AREA. 

On  the  south  side  of  the  narrow  band  of  Huronian  slates  which  has 
been  designated  as  the  w Eureka  Series,”  the  greenstones  of  the  Mar- 
quette area  present  a decided  contrast  to  those  which  have  been 
described  in  the  previous  section  as  occurring  on  its  north  side.  They 
are,  for  the  most  part,  massive,  pale  green  in  color,  and  apparently 
homogeneous  in  structure.  Only  in  rare  instances  can  individual  min- 
erals be  detected  with  the  unaided  eye.  A schistose  structure  is  not 
uncommon  in  these  rocks,  but  it  is  evidently  a pressure  foliation,  while 
the  parallel  banding  or  striping,  so  frequent  in  the  greenstones  of  the 
northern  area,  is  altogether  absent.  A study  of  these  pale  green 
aphanitic  greenstones  seems  to  indicate  that  they  were  not  originally 
to  any  great  extent  tuff  deposits,  but  massive  flows  of  diabase,  which 
have  since  suffered  profound  chemical  and  structural  change  in  conse- 
quence of  having  been  subjected  to  intense  dynamical  action. 

In  addition  to  their  foliation,  they  are  fractured  and  brecciated  in 
various  degrees,  and  often  exhibit  a curious  spheroidal  or  lenticular 
parting,  for  which  no  perfectly  satisfactory  explanation  has  been  found. 

The  monotony  of  these  prevailing  aphanitic  greenstones  is  inter- 
rupted by  bands  of  more  coarsely  crystalline  and  less  altered  rocks, 
which  represent  basic  dikes  of  more  recent  origin. 

THE  AFHANITIC  GREENSTONES. 

The  general  character  of  these  widely  distributed  rocks  as  seen  under 
the  microscope,  is  shown  in  PI.  X,  fig.  2,  drawn  from  a specimen  col- 
lected near  the  town  of  Negaunee,  where  this  type  is  developed  even 
better  than  near  Marquette.  In  the  mass  which  appears  to  the 
unaided  eye  as  quite  homogeneous,  the  microscope  discloses  long, 
almost  acicular  feldspar  crystals,  embedded  in  a confused  aggregate  of 
hornblende  needles,  chlorite  scales,  epidote,  quartz,  calcite,  and  cloudy 
spots,  probably  derived  from  leucoxene.  The  feldspar  in  these  rocks 
is,  as  a rule,  fresh,  and  their  twinning  lamellae  are  still  distinctly  visible. 
Some  of  the  more  acicular  crystals  seem  divided  at  the  ends,  as  is  so 
often  the  case  in  semi-vitreous  surface  rocks  whose  feldspar  microliths 
are  not  completely  formed.  Indeed,  in  many  of  their  characters,  these 
aphanitic  greenstones  strongly  resemble  porphyrites  or  melaphyres 


164 


GREENSTONE  SCHIST  AREAS  OF  MICHIGAN. 


[BULL.  62. 


whose  glassy  base  has  been  completely  transformed  into  an  aggregate 
of  secondary  products.  Tneir  structure,  imperfectly  preserved  as  it  is, 
strongly  indicates  a superficial  origin. 

As  typical  representatives  of  these  homogeneous  pale  green  rocks 
may  be  mentioned : No.  11638,  from  the  mouth  of  Whetstone  Brook, 
just  south  of  Marquette ; Nos.  11725  and  11726,  from  the  summit  of 
the  hill  immediately  south  of  the  last  locality ; No.  11694,  collected 
about  an  eighth  of  a mile  south  of  the  State  road  on  the  line  between 
the  southeast  and  southwest  quarters  of  Sec.  27,  T.  48  N.,  R.  25  W.;  and 
No.  11721,  from  south  of  the  township  road,  on  the  line  between  Secs. 
27  and  28,  T.  48  N.,  R.  25  W. 

These  aphanitic  greenstones  appear  to  have  been  particularly  sensi- 
tive to  dynamic  action.  We  find  locally  developed  in  them  every  de- 
gree of  pressure  foliation  from  a coarse,  slickensided  breccia  to  a chlo- 
ritic  slate.  The  cleavage,  however,  is  developed  parallel  to  a line  rather 
than  parallel  to  a plane,  as  is  the  case  with  a true  bedding.  There  is  a 
tendency  to  break  into  rhomboidal  prisms  or  along  almost  any  plane 
which  is  parallel  to  the  average  direction  of  dip. 

No.  11696  is  a much  gashed  and  brecciated  greenstone  which  adjoins 
on  the  north  an  uralite  diabase  dike,  No.  11695  (see  p.  169).  It  is  both 
schistose  and  chloritic,  but  its  microscopical  structure  shows  plainly 
that  it  was  once  a diabase,  and  that  its  present  character  is  due  en- 
tirely to  the  action  of  some  great  mechanical  force.  The  typical  ophitic 
structure  or  irregular  network  of  lath-shaped  feldspar  crystals  is  still 
readily  discernible.  The  mechanical  action  seems  to  have  been  rather 
a stretching  than  a compression.  The  feldspar  crystals,  which  are  con- 
siderably altered,  are  broken  and  the  fragments  pulled  apart.  The 
secondary  chlorite,  so  common  in  all  stretched  rocks  (cf.  PI.  XI,  fig. 
2),  is  here  abundant  in  the  numerous  longitudinal  cracks,  which  traverse 
the  rock  irrespective  of  its  component  minerals.  This  is  always  ar- 
ranged with  its  scales  or  fibers  perpendicular  to  the  walls  of  the  fissure. 

In  addition  to  such  brecciated  rocks  as  the  last  specimen,  very  per- 
fectly schistose  varieties  of  these  aphanitic  greenstones  are  common  in 
the  southern  part  of  the  Marquette  area,  their  strike  conforming  to  that 
of  all  the  other  rocks  of  this  region.  These  are  typically  exposed  at 
the  mouth  of  Whetstone  Brook  (Nos.  11639  to  11643);  in  the  railroad 
cutting  just  west  of  it  (No.  11645);  on  the  high  hill  still  farther  west- 
ward (No.  11726);  and  in  the  Duluth,  South  Shore  and  Atlantic  Rail- 
road cutting  just  north  of  the  Marquette  sandstone  quarries  (No.  11691). 

For  the  most  part,  these  rocks  are  a fine  chloritic  mass,  which,  under 
the  microscope,  shows  a pronounced  schistose  structure,  but  only  rarely 
any  certain  indications  of  eruptive  origin.  Very  faint  but  unmistak- 
able traces  of  the  ophitic  structure  are  nevertheless  sometimes  visible 
even  in  these  rocks,  as,  for  instance,  in  No.  11726,  which  was  entered 
in  the  field  notes  as  a “slaty  band  traversing  the  massive  greenstones 
above  Whetstone  Brook.” 


Williams. ] LOSSEN’s  WORK  ON  THE  GERMAN  GREEN  SCHISTS.  165 

The  history  of  these  schistose  greenstones  must  be  deciphered  with 
the  conjoint  evidence  afforded  by  the  microscope  and  a study  of  their 
relations  in  the  field.  The  occasional  survival  of  the  characteristic 
diabase  structure  even  in  some  of  the  more  foliated  forms,  taken  in 
connection  with  their  evident  identity  with  and  gradual  transition  into 
the  massive  varieties,  appears  to  be  sufficient  proof  that,  with  the 
exception  of  certain  unimportant  tuff  deposits,  these  green  schists  have 
been  derived  from  basic  eruptives  through  the  agency  of  intense  me- 
chanical and  chemical  action. 

The  closest  analogy  to  the  rocks  of  the  southern  Marquette  green- 
• stone  area  is  to  be  found  in  the  metamorphosed  diabases  of  the  eastern 
Hartz.  These  rocks  have  been  minutely  studied  and  for  the  first  time 
successfully  deciphered  by  K.  A.  Lossen,  of  Berlin.  His  descriptions 
could  be  applied  almost  verbatim  to  the  Marquette  greenstones ; and 
each  of  these  two  similar  areas  can  but  have  additional  light  thrown 
upon  its  interpretation  by  the  facts  afforded  by  the  other.1  Lossen  dis- 
tinguishes between  the  coarse  grained  or  granular  (kornig)  and  the 
fine  grained  (aphanitisch)  diabase,  as  has  been  done  in  the  area  here 
under  discussion.  He  finds  that  both  rocks,  but  especially  the  apha- 
nitic  type,  are  very  sensitive  to  dynamic  action,  and  that  in  the  process 
of  mountain  making  they  have  been  to  a large  extent  passively  meta- 
morphosed and  converted  into  breccias,  “Flaser”  diabase  and  green 
schists.  The  last  named  u grime  Schiefer  ” are  of  particular  interest 
to  us  on  account  of  their  resemblance  to  the  schistose  rocks  of  the 
southern  Marquette  area.  In  the  Hartz  they  make  a conformable  mem- 
ber of  the  Wieder  schists  (hercynian)  which  are  of  very  considerable  ex- 
tent and  are  always  associated  with  the  aphanitic  diabase.  The  minute 
and  careful  studies  of  Lossen  have  led  him  to  the  conclusion  that  these 
schists  are  not  in  any  way  sediments  nor  even  diabase  tuffs  (u  Sehal- 
steinev),  but  molecularly  metamorphosed  eruptive  rocks,  of  a fine 
grained  diabase  type.2  The  more  massive  rocks  are  considered  to  rep- 
resent old  lava  flows  which  occurred  while  the  accompanying  sedi- 
ments were  being  deposited,  and  the  idea  that  the  green  schists  of  the 
Wieder  horizon  were  once  also  massive  diabases,  is  based  both  upon 
the  field  relations  of  these  rocks  and  more  especially  upon  the  frequent 
remains  of  the  diabase  structure  which  they  still  contain. 

The  published  descriptions  of  many  other  green  schist  areas  in  Eu- 
rope— notably  in  Bavaria,  Saxony  and  the  Taunus — show  that  they 
possess  a strong  resemblance  to  those  of  Michigan  and  the  Eastern 
Hartz,  and  it  is  not  improbable  that  they  also  may  have  had  a similar 
origin. 

1 The  descriptions  of  Lossen  are  contained  in  the  explanations  to  the  special  geological  map  of  Prus- 
sia and  Thuringia  (Erlauterungen  zur  geologischen  Spocialkarte  von  Preussen  und  den  tjiiiringischon 
Staaten)  sheets  Pansfelde  (1882),  and  Wippra  (1883). 

2"  Dio  raikroskopische  Untersuchung  characteristischor  Vorkommen  dioser  typisclion  Diabas- 
aphaniten  vergesellschafteten  griinen  Schiefer  hat  orgeben,  dass  sie,  wenn  niclit  insgesammt,  doch 
grossentheils  als  unter  Drackschieferunj'Mrnolecular  umgeioandelte  Diabase  aufziifassen  sind.”  Ibid., 
Bl.  Wippra,  p.  27 ; (cf.  also  p.  46  and  Bl.  Pansfelde,  p.  52). 


166 


GREENSTONE  SCHIST  AREAS  OF  MICHIGAN. 


[BULL.  62. 


A noteworthy  feature  of  the  aphanitic  greenstones  and  greenstone 
schists  of  the  southern  Marquette  area,  and  one  which  is  exhibited  in 
a still  more  marked  degree  by  the  similar  rocks  occurring  near  the 
town  of  Negaunee  (see  the  following  section),  is  their  frequent. division 
into  spheroidal,  ovoid,  lenticular  or  more  irregularly  shaped  masses. 
These  differ  very  much  in  size,  as  well  as  form,  and  often  show  a tend- 
ency to  fit  together  like  stones  in  a mosaic,  although  they  are  always 
separated  by  interlacing  bands  of  a softer,  more  schistose  and  gener- 
ally darker  material.  These  anastomosing  bands  seem  to  wind  about  the 
harder  and  more  massive  cores,  becoming  thinner  or  thicker  according 
as  the  masses  approach  each  other  more  closely,  or  are  more  widely 
separated  by  the  rounding  off  of  their  corners.  This  peculiar  struct- 
ure, which  appears  to  be  only  local  in  its  development,  may  be  seen  at 
the  mouth  of  Whetstone  Brook  in  Marquette,  near  Baldwin’s  kilns,  near 
Negaunee  (NE  J of  NW  J of  Sec.  28  W.,  T.  48  N.,  R.  26  W.),  and  on  the 
south  side  of  the  Carp  River  along  the  logging  road  leading  northward 
from  the  east  end  of  Teal  Lake.  The  accompanying  diagram  (Fig.  26), 
drawn  from  the  last  named  exposure,  illustrates  the  general  character 
of  this  structure. 


Fig.  26. — Diagram  to  illustrate  spheroidal  parting  in  aphanitic  greenstone.  Carp  Kiver. 

Scale,  3 feet  to  the  inch. 

The  cores  generally  seem  to  be  quite  massive,  but  in  some  cases  they 
have  a latent  foliation  which  is  developed  by  weathering.  Where  the 
rock  has  become  decidedly  schistose,  as  was  observed  in  one  part  of 
the  Carp  River  exposure,  these  cores  are  pulled  out  into  long  interlock- 
ing lenses,  which  have  their  longest  axes  parallel  to  the  foliation.  (See 
Fig.  27,  p.  177.) 

Such  a structure  as  that  above  described  appears  to  be  not  uncom- 
mon in  the  greenstones  and  greenstone  schists  of  the  Northwest.  It 
is  well  known  to  the  Canadian  geologists,  who  have  designated  the 
rocks  exhibiting  it  as  “concretionary  traps.”  It  is  described  by  Dr. 
Andrew ‘C.  Lawson,  in  his  report  on  the  Lake  of  the  Woods,  in  the  fol- 
lowing terms : 

This  structure  consists  of  the  rock  being  divided  into  moreor  less  irregularly  spheri- 
cal or  ovoid  masses,  varying  iu  diameter  from  2 to  3 inches  to  as  many  feet.  These 
ovoid  masses  are  not  in  close  contact,  but  are  separated  from  one  another  by  an  in- 


WILLIAMS'.  1 


SPHEROIDAL  PARTING  IN  THE  GREENSTONES. 


167 


terstitial  material.  Tlie  concretionary  masses  are  at  their  points  of  nearest  approx- 
imation to  each  other,  generally  about  half  an  inch  or  an  inch  apart,  no  matter  what 
may  be  their  size,  so  that  when  the  ovoid  masses  are  large,  the  interstitial  material 
appears  in  section  as  thin,  anastomosing  sheets,  in  which  is  developed  a schistosity 
parallel  to  the  outlines  of  the  ovoid  masses  they  inclose.  The  interstitial  filling  is  gen- 
erally of  a darker  color,  more  chloritic,  softer,  and  of  a finer,  more  homogeneous  texture 
than  the  ovoid  masses,  and  weathers  out,  often  leaving  the  latter,  in  sect  ions  afforded 
by  glaciated  surfaces,  surrounded  by  sharp  little  trenches. 

The  ovoid  masses  are  uniformly  arranged  as  regards  the  direction  of  their  long  axes, 
and  each  one  is  surrounded  by  a sharp  border  half  an  inch  wide,  of  a dark  greenish 
gray  color,  which  has  been  more  resistant  to  weathering  agencies  than  the  rest  of 
the  rock.  The  ovoid  masses  present  as  the  result  of  weathering  a rough  or  pimpled 
surface  of  porous  aspect  and  bleached  greenish  white  color.  The  interstitial  filling 
is  firmer  in  texture  and  softer  than  either  the  ovoid  masses  or  their  border,  and  is 
intermediate  between  them  in  color,  with  a brownish  yellow  tinge. 

In  the  hornblende  schists  this  ovoid  structure  in  the  rock  takes  a somewhat  different 
aspect,  and  presents  the  appearance  of  thin  anastomosing  sheets  of  dark  green,  soft 
chloritic  material,  sometimes  enveloping  completely  ovoid  or  irregularly  shaped  por- 
tions of  the  hornblende  schist,  and  at  others  losing  themselves  in  a tapering,  dis- 
connected fashion  in  the  main  mass  of  the  rock.1 

It  is  evident  upon  the  most  superficial  examination  that  this  struct- 
ure is  in  no  way  “ concretionary ,w  as  that  term  is  commonly  under- 
stood. Nor  is  it  possible  to  suppose  that  the  harder  ovoid  masses  were 
originally  ejected  fragments,  which  have  become  imbedded  in  a finer 
matrix  of  volcanic  material  forming  a true  agglomerate.  A sufficient 
objection  to  this  hypothesis  is  the  fact  that  these  harder  masses  so 
frequently  fit  together  like  parts  of  a mosaic. 

In  many  instances  the  spherical  or  ovoid  form  of  the  disjointed 
fragments  is  so  perfect  that  the  structure  strongly  resembles  the 
spheroidal  parting,  developed  in  a latent  form  in  eruptive  rocks  by 
cooling,  and  made  more  distinct  by  weathering.  This,  which  is  really 
a perlitic  structure  on  a large  scale,  frequently  extends  through  large 
masses  of  eruptive  material  5 and  the  descriptions  and  photographs 
kindly  furnished  the  writer  by  Mr.  Whitman  Cross,  who  has  studied  it 
in  Colorado,  indicate  many  points  of  striking  resemblance  to  the  struct- 
ure of  the  Lake  Superior  greenstones.  It  is  quite  possible  that  the 
phenomenon  may  in  certain  cases  be  due  to  contraction,  although  in 
others  the  irregular  shape  of  the  fragments,  as  well  as  their  occurrence 
in  fragmental  rocks,  indicates  another  origin. 

A structure  showing  many  points  of  resemblance  to  that  here  de- 
scribed is  presented  by  the  well  known  green  schists  (griine  Schiefer), 
occurring  near  Hainichen,  in  Saxony,  and  the  explanation  afforded  by 
the  study  of  their  very  favorable  exposures  may  assist  our  understand- 
ing of  the  parting  in  the  Lake  Superior  greenstones.  The  fragments 
of  the  Saxon  green  schists,  in  spite  of  the  great  difference  in  their  size 
(varying  from  that  of  a pea  to  that  of  a house),  are  so  rounded  that  they 
were  formerly  regarded  by  C.  F.  Nauruan n as  a conglomerate.2  Never- 


1Geol.  and  Nat.  History  Survey  of  Canada,  Annual  Report  for  1885  (new  series,  Vol.  1);  Report 
CC  on  the  Lake  of  the  Woods,  by  A.  C.  Lawson,  pp.  52,  53. 

2Erlauterungen  zur  geogn.  Karte  des  Konigreichs  Sachsen,  pt.  1,  1834,  p.  09. 


168 


GREENSTONE  SCHIST  AREAS  OF  MICHIGAN. 


I BULL.  62. 


theless  tlieir  fitting  together  convinced  subsequent  observers  that  the 
structure  must  be  due  to  brecciation  in  situ.1  These  rocks  have  more 
recently  been  carefully  studied  by  A.  Rothpletz,  who  was  able  to  trace 
the  structure  downward  into  a series  of  interlacing  joints,  and  who  ex- 
plains the  rounded  character  of  the  fragments  and  the  production  of 
much  of  the  interstitial  material  by  the  rubbing  together,  under  the 
•action  of  intense  orographic  pressure,  of  a mass  already  finely  subdi- 
vided by  cracks.  Fig.  4 of  Rothpletz’s  plate  gives  a fair  representation 
of  some  of  the  Lake  Superior  occurrences.2 

The  hypothesis  of  the  mechanical  origin  of  this  curious  parting  in  the 
greenstones  and  greenstone  schists  seems  best  to  explain  the  following 
facts : 

(1)  Its  occurrence  in  fragmental  rocks. 

(2)  The  often  very  irregular  shape  of  the  fragments. 

(3)  The  interlocking  of  the  same  into  a mosaic. 

(4)  The  fact,  noticed  by  Lawson,  that  the  thickness  of  the  interstitial 
layer  is  independent  of  the  size  of  the  fragments. 

(5)  The  fact,  also  noticed  by  the  same  observer,  that  the  interstitial 
layer  in  horneblende  schists  often  loses  itself  in  the  rock  without  com- 
pletely surrounding  a fragment. 

(6)  The  identity  in  petrographical  character  of  all  the  cores  in  the 
same  mass. 

(7)  The  similarity,  except  where  it  is  more  altered,  of  the  interstitial 
material  to  that  forming  the  ovoid  cores.  At  the  Carp  River  locality 
(see  p.  176)  the  cores  contain  small  white  feldspar  crystals,  which  are 
also  present  in  the  layers  which  separate  them. 

COARSE  GRAINED  DIKE  ROCKS. 

The  fine  grained  aphanitic  greenstones  and  greenstone  schists  which 
prevail  over  the  southern  Marquette  area  are  intersected  by  many  bands 
of  coarser  material  whose  eruptive  character  is  still  evident  in  their 
microscopic  structure.  These  represent  later  dikes  of  a basic  character 
which  have  broken  through  the  older  rocks,  and  which  on  account  of 
their  more  recent  eruption  are  less  altered.  One  of  the  most  typical  of 
these  is  exposed  on  the  small  island  near  the  end  of  the  Cleveland  ore 
dock  in  Marquette.  This  small  island  consists  of  two  portions  con- 
nected by  a narrow  neck.  The  southern  part  is  composed  of  a hard, 
compact,  brown  rock,  which  is  sometimes  quite  coarse  grained  or  por- 
phyritic.  Its  color  and  the  abundance  of  epidote  which  is  macroscop- 
ically  visible  indicate  extensive  alteration.  Under  the  microscope  a 
specimen  from  this  locality,  No.  11649,  is  seen  at  a glance  to  be  a typ- 
ical diabase.  Although  every  vestige  of  the  original  pyroxene  has  been 

1 Naumann  : Erlauterungen  der  geogn.  Karte  der  Umgegend  von  Hainichen  im  Konigr.  Sachsen 
1871,  p.  11.  Rud.  Credner:  Das  Griinschiefersystem  von  Hainichen,  Zeitschr.  fur  die  gesammten, 
Naturwiss.,  vol.  47,  p.  127, 1876. 

2Ueber  mechanische  Geateinsuanwandlungen  bei  Hainichen  in  Sachsen,  part  2.  Zeitschr.  Deutsch. 
geol.  Gesell.,  vol.  31,  pp.  374-397.  PI.  IX,  1879. 


WILLIAMS.] 


DIABASES  SOUTH  OF  THE  MARQUETTE. 


169 


replaced  by  a finely  fibrous  green  hornblende  (uralite),  yet  the  char- 
acteristic ophitic  or  diabase  structure  is  still  perfectly  preserved.  The 
lath-shaped  feldspar  crystals  are  but  slightly  altered  and  the  spaces 
between  them  are  as  sharply  defined  as  when  the  rock  first  solidified. 

The  northern  portion  of  this  little  island  shows  the  same  diabase  in  a 
much  more  altered  form.  The  rock  has  a pale  greenish  color,  and,  though 
quite  massive  in  the  center,  is  schistose  on  either  side. 

Nos.  11651  and  11652,  the  former  from  the  massive  and  the  latter  from 
the  schistose  portion  of  this  rock,  offer  additional  examples  of  the  fact  so 
frequently  observed  in  the  Menominee  River  greenstones,  viz,  that  the 
feldspar  of  those  rocks  which  have  been  subjected  to  the  greatest  pres- 
sure is  more  broken,  but,  as  a rule,  less  altered  than  that  in  rocks  which 
have  experienced  less  violent  mechanical  action.  Both  of  these  speci- 
mens show  positive  evidence  in  their  structure  that  they  were  once 
diabases.  In  both  the  ophitic  arrangement  of  the  constituent  minerals 
is  still  distinct,  but  in  the  more  massive  rock  the  chemical  alteration  has 
progressed  much  further  than  in  the  other.  Here  the  lath-shaped  feld- 
spar crystals  are  preserved  in  outline  by  the  various  secondary  prod- 
ucts which  supply  their  place.  Fibrous  hornblende  and  leucoxene  are 
abundant  and  nowhere,  in  either  the  thin  section  or  hand-specimen,  is 
there  visible  any  parallelism  of  arrangement  among  the  components. 
In  the  schistose  rock,  on  the  other  hand,  chlorite  has  largely  replaced 
the  hornblende,  but  the  feldspar  is  almost  unaltered.  The  long,  lath- 
shaped crystals  are  broken  and  faulted — the  fragments  of  a single  indi- 
vidual often  being  separated  a considerable  distance — but  in  spite  of 
this  the  substance  is  as  fresh  and  the  twinning-lamellae  are  as  sharp  as 
in  a recently  solidified  rock.  Few  better  examples  could  be  found  of  the 
evident  action  of  pressure  upon  a solid  rock  mass.  There  has  been  a 
crushing  and  a consequent  development  of  schistose  structure  which 
the  microscope  reveals  with  great  distinctness.  Along  lines  where  an 
actual  slipping  took  place,  fibrous  hornblende,  chlorite,  and  calcite  have 
been  quite  abundantly  developed. 

No  more  typical  exposure  of  the  greenstones  of  the  southern  Mar- 
quette area  can  be  found  than  that  seen  in  the  high  hill  which  rises 
between  Whetstone  Brook,  the  State  road,  and  the  railroad.  (D  on  the 
map,  PI.  VII.)  The  freshest  rock  obtained  from  the  summit  of  this  hill, 
No.  11724,  is  one  of  the  best  preserved  diabases  found  anywhere  south 
of  the  Eureka  series.  The  feldspar  is  perfectly  fresh  but  is  much 
broken  and  faulted,  as  in  the  specimen  (No.  11652)  last  described.  The 
interstices  between  the  fragments  are  filled  with  chlorite.  The  allo- 
triomorphic  pyroxene  is  now  largely  replaced  by  paramorphic  horn- 
blende, although  cores  of  the  original  mineral  are  not  infrequent  in  the 
center  of  the  hornblende  areas.  Apatite,  ilmenite,  and  leucoxene  are 
also  present. 

Nos.  11646,  from  the  southwest  corner  of  the  railroad  crossing  on  Front 
street,  Marquette  (see  on  the  map,  PI.  VII.),  and  11695,  collected  just 


170 


GREENSTONE  SCHIST  AREAS  OF  MICHIGAN. 


[bIill.  62. 


north  of  the  state  road  (in  the  center  of  Sec.  27  T.  48  N.,  R.  25  W.),  are 
also  well  defined  uralite  diabases.  In  both  the  structure  is  still  intact 
and  the  feldspars  are  generally  well  preserved,  though  the  augite  is  wholly 
uralitized.  One  rock  of  exceptional  character  (No.  11687)  which  oc- 
curs within  the  limits  of  the  southern  Marquette  area,  must  not  be 
passed  over  without  notice.  This  outcrops  in  a small  exposure  at  the 
end  of  the  road  leading  westward  from  Marquette  to  the  Eureka 
shaft,  about  two  miles  from  the  city  (see  map,  PI.  VII).  It  is  of  a light 
brownish  color,  and,  in  spite  of  an  advanced  state  of  chemical  altera- 
tion, it  shows  plainly  the  effects  of  great  pressure.  It  appears  once 
to  have  been  a gabbro,  very  similar  to  that  occurring  at  Sturgeon 
Falls,  on  the  Menominee  River  (see  p.  67),  but  now  its  original  compo- 
nents and  structure  have  both  disappeared.  Interlacing,  lenticular 
areas  produce  a decided  “microflaser”  structure,  which,  in  places, 
even  resembles  the  fluidal  appearance  of  certain  vitrophyres.  The  min- 
erals now  present  are  a very  pale  chlorite  filled  with  sharp  epidote  or 
zoisite  needles,  saussurite,  quartz,  calcite,  ilmenite,  leucoxene  grains, 
and  winding  bands  of  a clear,  brown,  isotropic  substance  which  looks  like 
opal.  This  rock  appears  much  shattered  in  the  field  and  it  is  in  imme- 
diate contact  with  the  thin,  fissile  schists  in  which  the  Eureka  sbaft  is 
sunk. 

GREENSTONES  SOUTH  OP  THE  QUARTZITE. 

Some  distince  south  of  the  Carp  River,  in  the  west  half  of  the  NW. 
^ Sec.  6,  T.  47  N.,  R.  24  W.,  below  the  limestones  and  quartzite,  a few 
much  contorted  and  altered  greenstones  appear  just  on  the  contact 
with  the  granite  which  incloses  the  Marquette  basin  on  the  south. 

No.  11778  may  still  be  recognized  as  a diabase,  though  it  now  con- 
tains only  saussurite,  chlorite,  epidote,  quartz,  and  leucoxene. 

Nos.  11774  and  11775  are  from  the  same  greenstone  band,  the  former 
massive,  the  latter  schistose.  They  do  not  resemble  any  other  rocks  in 
the  Marquette  area,  but  they  find  their  analogues  in  certain  remarkable 
rocks  on  the  south  bank  of  the  Carp  River,  where  this  is  crossed  by  the 
road  leading  noithward  from  Teal  Lake  (see  succeeding  section,  p.  175). 
Sharply  defined  crystals  of  reddish  feldspar  are  imbedded  in  a bright 
green  mass  of  chlorite  and  serpentine.  The  feldspars,  although  not 
pulled  apart  as  in  rocks  which  have  been  subjected  to  a stretching,  show 
evidences  of  the  action  of  enormous  pressure.  Remnants  of  hornblende, 
from  which  the  serpentine  was  probably  derived  ; ilmenite,  surrounded 
by  leucoxene ; and  round  grains  of  bright  red  iron  hydroxide  are  also 
present  in  this  rock.  In  the  schistose  modification,  the  constituents  are 
pulled  out  into  parallel  bands.  The  feldspars  are  lath-shaped  and 
smaller,  and,  without  any  loss  of  sharpness  in  their  outline,  they  are  re- 
placed by  calcite,  which  is  surrounded  by  an  opaque  black  rim.  Cer- 
tain bands  in  this  rock  are  much  finer  grained  and  present  the  feldspar 
and  hornblende  in  a much  less  altered  condition. 

No.  11779,  from  this  same  locality,  is  one  of  the  best  specimens  any- 


171 


williams.  1 APHANITIC  GREENSTONES  NORTH  OF  NEGAUNEE. 

where  collected  to  show  the  effects  of  rock-stretching.  It  appears  once 
to  have  been  a granite  porphyry,  but  is  now  very  schistose  and  is  col- 
ored green  by  the  secondary  chlorite.  Its  ground  mass  is  a felt-like  ag- 
gregateof  sericite,  quartz,  and  chlorite  with  a perfectly  parallel  arrange- 
ment of  the  constituents.  The  large  porphyritic  feldspar  crystals  are 
much  broken  and  pulled  apart,  always  in  the  direction  of  the  folia- 
tion, as  shown  in  PI.  XIV,  fig.  2.  Large  calcite  individuals  are  sur- 
rounded by  bright  green  chlorite,  and  both  of  these  minerals  may  rep- 
resent original  biotite  or  some  bisilicate. 

ROCKS  OF  THE  NEGAUNEE  AREA. 

As  has  already  been  stated  at  the  beginning  of  the  preceding  chap- 
ter, two  points  were  selected  for  the  study  of  the  more  western  portion 
of  the  Marquette  greenstone  belt.  One  of  these  was  the  mining  town 
of  Negaunee,  situated  at  the  southeast  corner  of  Teal  Lake,  about 
twelve  miles  west  of  Lake  Superior.  The  town  itself  is  on  the  iron- 
bearing Huronian  rocks,  south  of  the  greenstone  belt,  whose  south- 
ern edge  skirts  the  northern  shore  of  Teal  Lake.  Both  east  and 
west  of  the  lake  the  greenstones  are  bounded  on  the  south  by  the 
narrow  ridge  of  white  quartzite,  whose  termination  is  Mount  Mesnard. 

From  this  quartzite  two  sections,  three  miles  apart,  were  run  north- 
ward to  the  granite  and  Huronian  rocks,  which  here  divide  the  green- 
stones into  two  separate  areas.  The  more  southern  of  these,  which  we 
will  designate  as  the  Negaunee  area,  resembles  in  its  general  character 
the  region  south  of  the  Eureka  series  near  Marquette;  while  the  region 
north  of  the  Dead  Biver,  which  will  form  the  subject  of  the  succeeding 
section,  is  much  more  like  the  northern  Marquette  area. 

The  greenstones  occupying  the  region  north  of  Negaunee  do  not 
occur  in  continuous  exposures,  but  rise  out  of  the  plain  composed  of 
glacial  and  later  deposits  in  the  form  of  rounded  knobs.  Both  the 
longest  axis  of  these  knobs  and  the  approximately  parallel  rows  in 
which  they  are  arranged  follow  the  east  and  west  strike,  common  to 
ail  the  rocks  of  this  region.  The  greenstones  are,  for  the  most  part,  of 
the  much  fissured  and  brecciated,  light  green  and  aphanitic  variety, 
described  in  the  last  section.  They  are  also  very  commonly  associated 
with  the  same  coarser  and  more  crystalline  eruptives,  probably  of  a 
much  later  age,  that  we  encountered  south  of  Marquette. 

As  will  be  readily  seen  from  an  examination  of  Dr.  BomingeFs  map 
the  Huronian  rocks  arbund  and  south  of  Negaunee  and  Ishpeming  are 
also  penetrated  by  numerous  greenstones.  These,  as  a rule,  resemble 
the  more  crystalline  and  later  intrusions  of  the  greenstone  belt  proper, 
and  they  may  have  been  contemporaneous  with  them. 

APHANITIC  GREENSTONES. 

The  main  mass  of  the  greenstone  belt  near  Negaunee  is  composed  of 
the  fine  grained  or  aphanitic  rock  which  has  been  described  in  the  last 


172 


GREENSTONE  SCHIST  AREAS  OF  MICHIGAN. 


[bull.  62. 


section  as  characteristic  of  the  region  south  of  Marquette.  They  be- 
long to  Lossen’s  type  of  “dichte  Diabase”  and  always  show  more  ad- 
vanced chemical  alteration  than  the  coarser  rocks.  This  is  to  be  ex- 
plained by  their  finer  grain  and  also  from  the  fact  that  they  are  older 
and  have  been  subjected  to  more  dynamic  action  than  the  others.  In 
the  field  these  rocks  are  found  to  be  much  brecciated  and  not  infre- 
quently quite  perfectly  foliated.  They  also  exhibit  the  peculiar  spher- 
oidal parting  already  described,  p.  166. 

The  microscopical  appearance  of  a fair  average  type  of  these  aphanitic 
greenstones  (No.  11747,  from  Baldwin’s  Kilns)  is  represented  in  PI.  X, 
fig.  2,  but  they  show  considerable  variation  in  both  structure  and  com- 
position. In  none  is  any  trace  of  pyroxene  now  to  be  found,  and  yet  they 
were  probably  once  typical  diabases.  Their  mineralogical  differences  are 
mainly  dependent  on  the  relative  proportions  of  hornblende  and  chlorite. 
The  preponderance  of  one  or  another  of  these  minerals  may-. be  attrib- 
uted to  a more  or  less  advanced  stage  of  chemical  alteration,  but  cer- 
tain differences  in  structure  have  probably  always  existed.  The  grain 
may  vary  considerably  in  its  coarseness,  while  the  long  acicular  feld- 
spar crystals,  so  abundant  in  some  specimens,  are  wholly  wanting  in 
others. 

No.  1 1736  was  collected  on  the  road  from  Negaunee  to  Baldwin’s 
Kilns,  just  beyond  the  Carp  River,  from  about  the  center  of  the  SW 
J of  the  NE  J of  Sec.  29,  T.  48  N.,  R.  26  W.  It  is  comparatively  coarse 
grained  and  little  altered.  Under  the  microscope  it  appears  as  a con- 
fused aggregate  of  fibrous  hornblende,  a cloudy,  opaque,  indetermin- 
able substance  and  some  original  feldspar  whose  crystals  are  much 
broken. 

No.  11744,  obtained  from  an  isolated  knob  of  greenstone,  situated  in 
the  S W J of  the  NE  J of  Sec.  28,  T.  48  N.,  R.  26  W.,  on  the  longer  road 
to  Baldwin’s  Kilns,  about  one  mile  east  of  where  the  last  specimen  was 
collected,  is  much  like  it  in  appearance  and  microscopic  character. 
The  only  differences  are  due  to  the  more  advanced  alteration  of  the  lat- 
ter rock.  Here  chlorite  is  abundant  and  the  feldspar  hardly  visible. 

No.  11745,  from  the  same  road  as  the  last,  but  much  nearer  the  Kilns, 
shows  the  spheroidal  parting  or  brecciatiou  in  a very  perfect  manner. 
The  grain  is  very  fine,  and  the  incomplete  skeleton-like  forms  of  por- 
phyritic  feldspar  crystals  are  numerous.  The  mass  itself  is  now  largely 
chloritic,  but  looks  as  if  it  might  once  have  been  a finely  porphyritic 
rock. 

No.  11747,  found  at  the  same  locality,  is  the  one  from  which  PI.  X, 
fig.  2,  was  drawn.  It  is  similar  in  structure  to  the  last  specimen,  but 
its  grain  is  coarser,  and  fibrous  hornblende  is  still  abundant  in.  its 
groundmass.  The  porphyritic  feldspar  crystals  are  broken,  faulted 
and  separated. 

No.  11748  is  a schistose  modification  of  11747.  This  rock  has  a much 
finer  grain  than  the  other,  but  no  evidence  of  schistose,  structure  is  ap- 


WILLIAMS.  | 


COARSE  GRAINED  GREENSTONES. 


173 


parent  under  the  microscope.  The  chemical  alteration  has  progressed 
so  far  that  hardly  any  of  the  substances  remaining  have  much  action 
on  polarized  light ; nevertheless,  faint  traces  of  small  acicular  feldspar 
crystals  are  visible. 

One  massive  greenstone,  No.  11740,  found  just  north  of  Baldwin’s 
Kilns,  in  the  NW  J of  Sec.  21,  T.  48  N.,  R.  26  W.,  is  striking  on 
account  of  its  being  mottled  with  round  white  spots  from  5mm  to  6mm 
in  diameter.  The  rock  is  somewhat  darker  than  usual  in  a rim  around 
these  spots,  and  the  whole  effect  is  exactly  that  of  a variolite.  Under 
the  microscope  the  rock  itself  is  found  to  be  composed  almost  wholly 
of  green  fibrous  hornblende,  together  with  some  opaque  grains  and 
saussurite.  The  round  whitish  spots  are  very  largely  composed  of 
saussurite  or  a very  fine  mosaic,  in  which  sharply  defined  hornblende 
crystals  are  imbedded.  They  do  not  show  the  least  trace  of  a radial 
or  sheaf-like  arrangement,  such  as  is  characteristic  of  a true  variolite. 
These  spots  are  not  unlike  those  found  in  the  banded  greenstones  of 
the  Brook  section  (see  p.  157)  in  their  composition  and  structure,  but 
they  are  very  much  more  regular  and  uniform  in  their  shape. 

Other  specimens  of  these  aphanitic  greenstones,  as  for  instance  Nos. 
11793,  11795,  11796,  and  11797,  collected  along  the  line  of  the  old 
logging  road,  which  leads  from  the  eastern  end  of  Teal  Lake  north- 
ward to  Johnson’s  Camp,  in  the  SE  £ of  Sec.  13,  T.  48  N.,  R.  27  W.,  are 
quite  like  those  above  described  from  the  neighborhood  of  Baldwin’s 
Kilns. 

COARSELY  CRYSTALLINE  GREENSTONES. 

No.  11749,  collected  in  the  extreme  northeast  corner  of  Sec.  21  T. 
48  N.,  R.  26  W.,  northeast  of  Baldwin’s  Kilns,  is  an  unusually  beauti- 
ful rock.  The  structure  is  coarse  grained  and  rather  granular,  in 
spite  of  the  feldspar  crystals  being  idiomorphic.  The  large  individuals 
of  hornblende  also,  to  some  extent,  have  their  characteristic  crystal 
form.  They  are  frequently  changed  to  chlorite  or  to  fibrous  horn- 
blende, but  still  oftener,  although  bleached  to  a pale  green  color,  they 
retain  their  compact  texture  and  show  a twinning  structure.  There 
are  no  present  indications  that  this  rock  ever  contained  pyroxene,  and 
it  is  therefore  to  be  designated  as  a diorite.  The  hornblende  shows, 
in  the  process  of  its-  alteration,  a curious  tendency  to  concentrate  the 
deep  green  color  around  the  periphery  of  the  crystals  ; also  the  fraying 
out  of  their  edges  into  hornblende  needles  similar  to  those  described 
by  Becke  and  Van  Hise  as  secondary  growths,  produced  by  regularly 
orientated  accretions  of  hornblende  substance.  All  of  these  features 
are  shown  in  Plate  XII,  fig.  1,  which  represents  the  microscopic  ap- 
pearance of  this  rock.  The  feldspar  is  filled  with  epidote  or  actinolite 
• needles.  Large  areas  of  bright  green  chlorite  also  occur  which  contain 
sometimes  sharp  epidote  crystals,  but  more  commonly  fibrous  horn- 
blende. Leucoxene  after  ihnenite  is  abundant. 


174 


GREENSTONE  SCHIST  AREAS  OF  MICHIGAN. 


[BULL.  GB. 


No.  11739,  from  the  southeasterly  portion  of  the  SW  ^ of  the  NW  J 
Sec.  21,  T.  48  N.,  E.  2(3  W.,  just  north  of  Baldwins  Kilns,  is  a dioritic 
rock  much  like  the  last,  but  it  is  considerably  more  altered.  The  horn- 
blende is  more  fibrous,  the  feldspar  more  saussuritized,  while  the 
original  structure  is  also  beginning  to  suffer. 

No.  11746  was  taken  from  a well  marked  dike  which  intersects  the 
spheroidally  parted,  aphanitic  greenstones,  near  Baldwin’s  Kilns.  Here 
the  diabase  or  ophitic  structure  is  perfectly  developed,  and  there  is 
no  reason  to  doubt  that  the  pale  green,  fibrous  hornblende,  which  now 
fills  the  allotriomorphic  spaces  between  the  lath-shaped  feldspar  crys- 
tals is  secondary  after  augite.  The  most  interesting  feature  of  this 
rock  is  its  amygdaloidal  structure  which  was  observed  in  no  other  Mar- 
quette greenstone.  Several  small  amygdules  are  filled  with  brightly 
polarizing  epidote,  while  one  large  circular  cavity,  measuring  four 
millimeters  in  diameter,  has  its  sides  coated  with  radiating  epidote 
needles  and  its  center  filled  with  calcite. 

No.  11741  is  the  rock  exposed  at  Baldwin’s  Kilns.  It  is  much  jointed 
but  quite  massive.  Under  the  microscope  it  appears  like  the  specimen 
last  described,  except  that  it  is  finer  grained  and  devoid  of  amyg- 
daloidal cavities.  The  structure  of  this  rock  is  perfectly  preserved. 
It  was  once  a typical  diabase,  although  now  no  trace  of  pyroxene 
remains. 

Another  of  the  more  coarsely  crystalline  dike  rocks  of  the  Negaunee 
greenstone  belt  was  obtained  near  the  granite  contact  in  Sec.  13,  T.  48 
N.,  E.  27  W.,  two  and  one-half  miles  north  of  Teal  Lake.  This  (No. 
11791)  is  a typical  uralite  diabase,  as  is  shown  both  by  the  distinct 
traces  of  ophitic  structure  and  by  the  frequent  cores  of  pale  reddish 
brown  augite  which  still  remain  in  the  fibrous  hornblende.  Ilmenite, 
partially  changed  to  leucoxene,  is  also  present  in  forms  especially  char- 
acteristic of  diabase.  The  original  structure  has  been  considerably 
obscured  by  chemical  changes.  The  feldspar  is  partly  recrystallized  to 
a mosaic,  and  epidote,  chlorite,  and  quartz  have  been  secondarily  de- 
veloped. 

As  has  been  above  remarked  (p.  171),  the  greenstones  which  occur  so 
abundantly  in  the  iron  bearing  Huronian  rocks  both  north  and  south  of 
Negaunee  are  apparently  identical  with  the  coarse  grained,  younger 
rocks  of  the  greenstone  belt  proper.  Still  they  show  the  effects  of  hav- 
ing been  subjected  to  enormous  pressure  which  has  frequently  produced 
in  them  a schistose  structure ; and  as  this  is,  in  every  case,  conformable 
to  the  general  strike  of  all  the  rocks  of  this  region,  we  must  conclude 
that  these  greenstones  were  intruded  before  the  folding  of  the  Huronian 
sediments  was  completed.1 

Specimens  were  collected  from  the  prominent  exposures  of  these 
greenstones  near  the  town  of  Negaunee.  They  are  ail  rather  coarse 
uralite  diabases  of  the  type  last  described  from  the  greenstone  belt. 


See  sections  by  Brooks,  Atlas  to  Geol.  Survey  Michigan,  Pis.  in  and  v. 


WILLIAMS.] 


CARP  RIVER  TUFFS. 


175 


No.  11754,  collected  from  the  SW  J of  the  SW  J Sec.  6,  T.  47  N.,  R.  26 
W.,  near  the  mouth  of  the  Jackson  mine,  has  a well  preserved  diabase 
structure.  Its  pyroxene  is  wholly  changed  to  pale  secondary  horn- 
blende ; its  feldspar  is  filled  with  epidote,  while  chlorite  and  leucoxene 
are  common. 

No.  11755,  from  a high  hill  somewhat  farther  east,  is  essentially  the 
same  rock.  It  contains  epidote  and  chlorite  even  more  abundantly. 

No.  11756  was  collected  from  a small  greenstone  knob  just  east  of 
the  hotel  (Breitung  House)  in  Negaunee.  This  rock  has  been  quarried 
and  may  be  plainly  seen  to  have  been  rendered  partially  schistose  by 
pressure.  Under  the  microscope  it  is  like  the  preceding  rocks  except 
that  alteration  has  here  progressed  further — so  much  so  as  to  have 
obscured,  though  it  has  not  obliterated,  the  original  diabase  structure. 
Chlorite,  epidote,  and  calcite  are  among  the  prominent  constituents. 

Nos.  11758  and  11759  are  from  the  greenstone  bluffs  which  skirt  the 
southern  shore  of  Teal  Lake  near  its  eastern  end.  The  former  is  the  most 
massive,  the  latter  a schistose  variety  of  this  exposure.  The  massive  rock 
is  a uralite  diabase  of  the  ordinary  type,  retaining  its  original  structure 
and  also  occasional  cores  of  red  augite  in  the  masses  of  secondary  horn- 
blende. Besides  the  usual  chlorite,  epidote,  and  leucoxene,  there  is  con- 
siderable quartz  present  in  this  rock.  The  second  specimen,  taken  from 
the  schistose  band  on  the  south  side  of  this  greenstone  ridge,  shows 
evidence  of  intense  mechanical  and  chemical  action.  The  original 
structure  has  almost  wholly  disappeared,  while  its  component  minerals 
are  calcite  and  chlorite,  together  with  a little  quartz  and  leucoxene. 
Rarely  these  secondary  products  have  preserved  the  outline  of  lath- 
shaped feldspars,  which  show  that  they  have  been  much  broken  and 
pulled  apart  by  the  stretching  action  to  which  the  rock  has  been  sub- 
jected. 

THE  STRETCHED  FRAGMENTAL  ROCKS  ON  THE  CARP  RIVER. 

An  enigmatical  group  of  rocks  was  met  with  near  the  center  of  the 
Negaunee  greenstone  belt,  where  the  old  road  leading  to  Johnson’s 
logging  camp  crosses  the  Carp  River.  This  locality  is  in  the  NE  £ 
Sec.  25,  T.  48  N.,  R.  27  W.  The  first  rock  south  of  the  river  is  exposed 
in  a low  wall  which  rises  just  west  of  the  trail.  (No.  11798.)  This  is 
apparently  a dark  colored,  schistose  greenstone,  standing  nearly  vertical 
and  filled  with  red  granite  fragments  of  all  shapes  and  sizes,  though 
generally  with  well  rounded  outlines.  The  dark  green  matrix  also  con- 
tains much  of  the  red  material  in  a finely  divided  form,  often  resembling 
sharp  crystals.  The  rock  itself  is  much  brecciated  and  cut  by  cross- 
gashes,  as  if  it  had  been  subjected  to  a stretching  tension. 

Under  the  microscope  the  dark  green  portion  of  this  rock  is  found  to 
consist  entirely  of  chlorite,  the  scales  of  which  are  arranged  parallel  to 
each  other  and  to  the  cleavage  planes  of  the  mass.  Its  color,  when  free 
from  inclusions,  is  a clear,  bright  green,  but  it  frequently  contains  con- 


176 


GREENSTONE  SCHIST  AREAS  OF  MICHIGAN. 


[BULL.  62. 


siderable  black  or  brownish  opaque  material,  which  is  arranged  in  long, 
sinuous  lines  following  the  foliation.  The  reddish  inclusions  are  almost 
altogether  orthoclase,  colored  by  a fine,  unevenly  distributed,  globu- 
litic  dust.  A striated  feldspar  may  also  be  occasionally  observed.  The 
orthoclase  is  partly  in  sharply  defined  crystals,  but  more  commonly  in 
irregular  and  angular  fragments.  These  range  through  all  sizes  down 
to  the  most  microscopic  dimensions.  The  smallest  bits  are  locally 
scattered  so  thickly  through  the  chlorite  as  to  give  the  rock  a decid- 
edly clastic  appearance. 

The  chlorite  matrix  is  of  that  peculiar  character  which  we  have 
already  had  occasion  to  notice  as  characteristic  of  stretched  greenstone, 
particularly  in  the  Menominee  Valley  (see  pp.  82, 83,  and  PI.  XI, 
fig.  2).  This  chlorite  must  have  crystallized  after  the  orthoclase  frag- 
ments had  come  into  their  present  relative  positions,  as  may  be  seen 
from  the  relations  of  its  scales  to  the  feldspar,  and  also  by  the  bending 
around  these  fragments  of  the  sinuous  bands  of  opaque  matter  which 
the  chlorite  sometimes  contains.  We  may  go  even  further  and  assert 
that  the  chlorite  could  not  have  been  formed  prior  to  the  stretching 
action.  Proof  of  this  is  to  be  found  in  the  fact  that  some  of  the  ortho- 
clase inclusions  may  be  plainly  Seen  to  have  been  broken  during  this 
process  and  their  fragments  to  have  been  separated  but  a short  dis- 
tance and  always  in  the  direction  of  the  foliation ; and  yet  the  same 
chlorite  which  forms  ths  whole  matrix  fills  these  late  fissures. 

It  is  impossible  to  state  auything  positive  with  reference  to  the  origin 
of  this  chlorite ; and  still  its  universal  presence  in  the  stretched  green- 
stones would  indicate  that  this  particular  form  of  dynamic  action  upon 
a mass  of  the  proper  chemical  composition  is,  in  some  way,  neces- 
sary, or  at  least  very  favorable  to  its  production. 

No.  11799,  from  the  same  locality,  is  essentially  like  the  last  speci- 
men, except  that  the  included  feldspar  is  lighter  colored  and  perhaps 
more  altered  to  kaolin  or  muscovite.  The  matrix  is  not  so  purely 
chloritic,  but  contains  much  finely  divided  feldspar.  The  stretching 
action  is  here  even  more  apparent,  a single  feldspar  crystal  being  pulled 
out  to  over  double  its  original  length  and  its  fissures  being  filled  with 
the  same  green  chlorite. 

If  we  trace  this  ridge  farther  south  it  develops  into  a finer  grained 
and  more  schistose  greenstone,  which  is  free  from  the  larger  granitic 
inclusions  but  is  mottled  with  small  white  spots  (No.  11800).  These  are 
found  upon  closer  examination  to  be  feldspar  crystals.  Under  the 
microscope  this  rock  is  quite  like  those  above  described,  but  it  shows 
much  more  distinctly  the  effects  of  dynamic  action.  The  grain  is  very 
uneven.  In  some  places  the  feldspar  crystals  are  thickly  crowded  and 
are  cemented  by  the  usual  chlorite  in  which  epidote  is  abundant;  in 
other  places  the  matrix  is  a very  fine  grained  aggregate  of  chlorite, 
sericite,  quartz,  and  feldspar,  containing  considerable  opaque  substance 
and  possessing  a micro-flaser  structure  produced  by  the  winding  of  its 


williams.]  EFFECT  OF  STRETCHING  ON  SPHEROIDAL  PARTING.  177 


parallel  bands  about  the  occasional  feldspar  inclusions.  These  latter 
are  much  pulled  out  in  the  direction  of  the  foliation  and  have  their 
interstices  filled,  sometimes  by  the  chlorite,  but  oftener  still  by  calcite. 

No.  11801  is  a more  weathered  specimen  of  this  same  rock,  which 
shows  with  great  distinctness  the  spheroidal  parting  described  above 
(see  p.  166).  The  stretching  action  is  here  displayed  by  the  pulling 
out  of  the  spheroids  into  a system  of  interlocking  lenses,  as  represented 
in  Fig.  27.  Under  the  microscope  this  rock  shows  the  effect  of  the  me- 


Fig.  27 — spheroidal  parting  of  aphanitic  greenstone  pro- 
duced by  brecciations;  drawn  out  into  lenses  by  pres- 
sure. Scale  same  as  in  Fig.  26. 


chanical  action  in  the  extremest  degree.  The  matrix  is  very  schistose 
and  consists  of  a gray,  indeterminable,  almost  isotropic  mass  in  which 
minute  flakes  of  sericite  are  distinguishable.  The  feldspar  crystals 
are  so  altered  that  they  seem  to  grade  imperceptibly  into  the  matrix, 
leaving  their  original  shapes  but  indistinctly  outlined.  The  dark  green 
chlorite  occurs  only  in  rare  patches. 

No.  11802  is  from  the  interstitial  mass  between  these  lenses.  It  is  a 
finely  fibrous,  felt-like,  sericitic  mass,  in  which  the  scales  are  so  strictly 
parallel  that  the  entire  slide  extinguishes  the  light  between  crossed 
Nicol  prisms  almost  like  a homogeneous  crystal.  There  are  besides  pres- 
ent only  small  patches  of  a light  brown,  isotropic  substance,  some  little 
quartz  in  isolated  areas,  and  long  stringers  of  leucoxene,  out  of  which 
minute  but  sharp,  highly  refractive  octahedrons  have  been  developed 
(anatase  ? cf.  No.  11130,  p.  131). 

No.  11803,  also  from  this  interstitial  material,  contains  white  feldspar 
crystals  like  the  more  massive  cores.  A microscopic  examination  shows 
that  this  specimen  is  in  all  respects  identical  with  the  rock  which  it  sur- 
rounds. The  schistose  structure  is  due  to  a crushing  accompanied  by 
a tension  in  one  direction.  The  effect  of  this  is  so  striking  on  the  in- 
cluded feldspar  crystals  that  it  has  been  selected  for  illustration.  (PI. 
XIV,  fig.  2.) 

After  a careful  study  of  this  suite  of  rocks,  which  is  distributed  over 
a considerable  area,  it  is  impossible  to  escape  the  conviction  that 
they  are  of  a fragmental  character.  Neither  their  structure  nor  their 

Bull.  02 12 


178 


GREENSTONE  SCHIST  AREAS  OF  MICHIGAN. 


[BULL.  62. 


mineral  composition  resembles  that  of  any  known  eruptive  rock  while 
the  sudden  variations  in  grain,  the  irregular  and  angular  shape  of  the 
feldspar  inclusions,  and,  above  all,  the  extreme  differences  in  the  size  of 
even  such  of  these  inclusions  as  lie  side  by  side  can  be  reconciled  only 
with  a clastic  origin.  Still  these  rocks  do  not  bear  the  stamp  of  true  sed- 
iments, and  the  most  probable  hypothesis  of  their  nature  which  the 
writer  can  offer  is  that  they  are  deposits  of  volcanic  ejectamenta  which 
have  subsequently  been  rendered  schistose  by  dynamic  agencies.  The 
irregular  and  angular  fragments  of  red  granite  must  be  regarded  as 
material  broken  from  off'  the  underlying  rock  masses  and  hurled  out  by 
the  violent  explosive  force,  along  with  much  finer  rapilli,  sand,  and 
ashes.  These  rocks  seem  to  agree  very  closely  with  the  agglomerates 
described  by  Mr.  A.  O.  Lawson,  of  the  Oanadiau  Geological  Survey,  as 
attaining  an  extensive  development  in  the  Lake  of  the  Woods  region. 
These  are  filled  with  angular  fragments  and  have  also  been  subjected 
to  great  pressure.  Mr.  Lawson’s  opinion  regarding  the  origin  of  these 
agglomerates  is  the  same  as  that  above  advanced. 1 

The  presence,  as  here,  of  the  spheroidal  or  lenticular  parting  in  rock 
of  fragmental  origin  is  sufficient  to  show  that  it  must  be  a mechanical 
and  not  a molecular  phenomenon. 

ACID  ROCKS. 

There  were  no  acid  intrusives  encountered  within  the  Negaunee  green- 
stone area  proper,  nor  do  the  granites  which  skirt  the  northern  edge  of 
this  belt  present  any  points  worthy  of  especial  note. 

No.  11790  is  the  granite  in  immediate  contact  with  the  greenstones  at 
the  end  of  the  section  which  was  run  northward  from  Teal  Lake.  It 
was  found  at  the  Johnson  logging  camp  in  Sec.  13,  T.  48  N.,  B.  27  W. 
This  is  a typical  granitite  in  which  quartz  is  not  very  abundant.  The 
biotite  is  quite  altered  and  bleached.  The  feldspar  is  particularly  dis- 
tinguished by  its  beautiful  zonal  structure,  which  the  incipient  kaoliniza- 
tion  has  brought  out  all  the  more  distinctly.  This  feldspar  shows  the 
effects  of  pressure,  and  in  one  instance  this  can  be  plainly  seen  to  have 
resulted  in  the  production  of  a microcline  structure.  One  small,  sharp  _ 
crystal  supposed  to  be  orthite  was  observed  in  this  rock.  Apatite  and . * 
zircon  also  occur,  and  occasionally  a few  rutile  needles  are  secondarily 
developed  in  the  altered  mica. 

No.  11738  is  from  the  granite  in  contact  with  the  greenstone  just  $ 
north  of  Baldwin’s  Kilns.  This  rock  is  completely  crushed,  the  constit-  j 
uents  being  in  some  cases  so  pulverized  as  to  give  the  specimen,  when 
seen  under  the  microscope,  almost  the  appearance  of  a fragmental  de-  j 
posit.  The  mica  is  here  much  altered,  and  among  secondary  products 
has  given  rise  to  an  abundance  of  most  delicate  rutile  needles,  which 
often  form  the  characteristic  twins. 


Geol.  and  Nat.  Hist.  Survey  of  Canada.  Ann.  Rept.  for  1885,  p.  49,  CC, 


WILLIAMS.] 


QUARTZITE  NOVACULITES. 


179 


Here  may  conveniently  be  recorded  some  observations  made  on  the 
quartzite  of  the  ridge  which  borders  the  greenstones  on  the  south  in  the 
neighborhood  of  Negaunee.  This  quartzite  mass  is  composed  on  its 
northern  or  lower  side  of  compact,  even  grained,  thinly  laminated 
rocks,  varying  in  color  from  black  to  the  lighter  shades  of  green,  yellow, 
and  drab.  At  one  point,  near  the  northeast  corner  of  Teal  Lake,  these 
have  been  quite  extensively  quarried  as  novaculites,  although  they  are 
of  a different  character  from  the  novaculites  occurring  near  Marquette. 
These  rocks  have  the  usual  east  and  west  strike  and  dip  steeply  to  the 
south.  These  so-called  novaculites  are  again  underlaid  by  conformable 
beds  of  a coarse,  white  quartzite  conglomerate,  which  in  its  turn  is  in 
immediate  contact  with  the  greenstones.  The  best  locality  for  seeing 
these  contacts  is  on  the  wood  road  leading  northeastward  from  the 
slaughter-house  on  Teal  Lake.  (NVY  J Sec.  31,  T.  48  N.,  E.  26  W.) 

No  11785  is  a nearly  black  specimen  of  the  novaculite.  Under  the 
microscope  the  fragmental  character  of  this  rock  is  at  once  apparent. 
It  is  composed  of  irregular  quartz  and  altered  feldspar  grains  in  nearly 
equal  proportions.  In  the  finer  cement  biotite  has  abundantly  crystal- 
ized.  An  occasional  zircon  crystal  would  seem  to  indicate  that  the  rock 
is  the  stratified  debris  of  an  old  granite.  The  present  foliation  of  these 
novaculites  is  to  be  regarded  as  a slaty  cleavage  due  to  pressure,  rather 
than  an  original  stratification. 

The  conglomerate  between  the  novaculite  and  greenstone,  and  form- 
ing the  base  of  the  Huronian  quartzite,  is  composed  of  large  grains 
and  pebbles  of  granitic  quartz,  imbedded  in  a fine,  silky  matrix  of 
sericite.  (Nos.  11787  and  11788.) 

ROCKS  OF  THE  NORTHERN  AREA. 

The  second  point  selected  for  the  examination  of  the  western  portion 
of  the  Marquette  greenstone  belt  is  near  the  center  of  Sec.  9,  T.  48 
N.,  E.  2G  W.  Here  a camp  was  established  and  from  it  were  studied 
the  greenstones  represented  upon  Dr.  Eominger’s  map  as  occurring 
north  of  the  Dead  Eiver.  The  rocks  within  this  area  present  a much 
more  varied  character  than  those  of  any  of  the  other  areas  examined. 
Indeed,  although  a considerable  collection  of  specimens  was  made,  it  is 
not  for  a moment  supposed  that  all  the  types  of  massive  rocks  which 
occur  in  this  region  were  obtained.  Enough,  however,  will  be  noticed 
to  indicate  the  general  character  of  the  area  and  at  the  same  time  to 
illustrate  the  extreme  variety  offered  by  different,  and  often  nearly 
contiguous,  outcrops. 

In  its  chief  features,  this  area  more  closely  resembles  the  northern 
portion  of  the  belt  near  Marquette,  just  as  the  southern  branch  near 
Negauuee,  as  stated  in  the  preceding  section,  is  more  like  the  south- 
ern Marquette  area.  Still,  the  more  recent  eruptive  rooks  which  pene- 
trate the  banded  green  schists  far  exceed,  both  in  amount  and  variety, 
those  to  be  found  nearer  Marquette. 


180 


GREENSTONE  SCHIST  AREAS  OF  MICHIGAN. 


[bull.  62. 


UNALTERED  BASIC  INTRUSIVES. 

At  the  falls  of  the  Dead  River,  in  the  southwest  corner  of  Section  9, 
the  “ arenaceous  slate  group”  of  Rominger  is  well  exposed.  This  con* 
sists  here  of  thinly  bedded  slates  which  strike  N.  75°  W.  and  stand 
nearly  vertical,  with  perhaps  an  inclination  to  the  south.  The  upper 
part  of  the  fall  is  a steep  incline  over  the  slates,  but  the  lower  portiou 
is  a clear  fall  of  from  twenty-five  to  thirty  feet,  occasioned  by  several 
trap  dikes  which  run  nearly  east  and  west.  These  are  coarse  grained, 
fresh,  and  sometimes  porphyritic. 

No.  11814,  from  one  of  these  dikes,  is  found,  under  the  microscope,  to 
be  a very  fresh  and  typical  olivine  diabase,  quite  like  that  of  the  great 
dike  on  Lighthouse  Point,  Marquette.  The  structure  is  typically 
ophitic.  The  porphyritic  appearance  is  occasioned,  not  by  single  indi- 
viduals of  feldspar,  but  by  concretionary  aggregates  of  this  mineral. 
The  olivine,  which  frequently  presents  crystal  outlines  of  great  sharp- 
ness, is  sometimes  completely,  sometimes  only  slightly  serpentinized. 

No.  11826  was  collected  from  an  outcrop  beside  the  road  at  the  south- 
west corner  of  Sec.  10,  T.  48  N.,  R.  26  W.  It  has  every  appearance  of 
being  in  place,  but  the  character  of  the  rock,  unknown  elsewhere  in  this 
region,  renders  it  much  more  probable  that  it  is  a portion  of  a huge  glacial 
erratic  which  is  nearly  buried  in  the  drift.  Still,  the  petrographical  in- 
terest of  this  rock  makes  it  worthy  of  a description.  A close  examina- 
tion shows  it  to  be  an  olivine  gabbro,  perfectly  fresh  and  peculiar  on 
account  of  the  abundance  and  beauty  of  its  olivine.  This  constituent 
makes  up  a large  percentage  of  the  entire  mass.  It  is  present  in  ex- 
tremely sharp  and  well  formed  crystals  from  0.1  to  lmra  in  diameter. 
These  show  the  usual  hexagonal  cross-sections,  due  to  the  presence  of 
faces  of  the  prismatic  zone  and  domes.1  No  signs  of  even  incipient 
alteration  are  visible  in  this  olivine.  The  augite  and  triclinic  feldspar 
are  both  allotriomorphic,  and  form  much  larger  individuals  than  the 
idiomorpliic  olivine  which  they  inclose.  Magnetite  is  abundant  in 
sharp  octahedral  crystals,  showing  quadratic  sections  ; while  other  ir- 
regular areas  of  an  opaque  black  iron  mineral  may  be  ilmenite.  These 
latter  are  often  partially  bordered  by  a dark  brown  mica.  No  other 
rock  exactly  like  this  is  known  to  me,  but  in  its  general  character  it  is 
allied  to  the  olivine  gabbros  which  play  such  an  important  role  on  the 
north  shore  of  Lake  Superior.2 

ALTERED  COARSE  GRAINED  ROCKS. 

The  coarser  grained  intrusive  rocks,  which  penetrate  the  prevailing 
green  schists  of  the  northern  area,  have,  as  a rule,  undergone  a consid- 
erable amount  of  chemical  alteration.  This  has  more  or  less  completely 
replaced  the  original  minerals  by  secondary  products  ; while,  in  some 


1 These  crystals  show  indications  of  twinning,  as  described  by  Kalkowsky  (Zeitsclir.  Kryst.  n.  Min- 
eral, vol.  10,  ]).  17)  but  these  are  not  as  distinct  as  the  sharpness  of  the  crystals  would  lead  us  to  expect. 
2 Of.  Irving;  Mon.  U.  S.  Geol.  Survey,  vol.  5. 


WILLIAMS.  J 


DIORITES  OF  THE  NORTHERN  AREA. 


181 


cases,  it  has  also  obliterated  the  original  structure.  Among  these 
younger  eruptive  greenstones  the  same  two  types  can  be  distinguished 
as  in  the  Marquette  area,  viz,  diorite  and  diabase. 

Diorite — Nos.  11828  and  11829  are  from  an  exposure  thirty  paces  in 
width,  on  the  line  between  Secs.  5 and  8,  T.  48  N.,  R.  26  W.  This  rock 
is  sometimes  parted  into  parallel  plates  so  as  almost  to  resemble  a slate. 
In  the  hand-specimen  it  is  seen  to  be  composed  of  rather  large,  well- 
formed  hornblende  crystals,  which  are  often  hollow  at  the  center,  and 
a reddish  feldspar.  The  microscope  shows  that  the  two  specimens  are 
identical.  The  hornblende  is  idiomorphic,  though  without  terminal 
planes;  the  feldspar,  on  the  other  hand,  is  wholly  allotriomorpkic. 
This  latter  mineral  is  almost  free  from  twining  striations,  so  that  the 
rock  were  perhaps  more  properly  termed  a syenite.  The  hornblende 
preserves  much  of  its  compact  structure  and  brownish  color.  It  is 
frequently  changed  at  the  center  to  a mass  of  fibrous  needles,  or  even 
to  chlorite,  while  the  exterior  remains  compact  and  unaltered.  Apatite 
is  very  abundant;  sphene  and  magnetite  are  not  uncommon. 

No.  11817,  from  a wide  dike  at  the  northwest  corner-post  of  Section 
9,  of  the  same  township,  is  of  the  same  type  as  the  last  specimens,  but 
more  altered.  Macroscopically  tufts  of  hornblende  crystals  may  be 
seen  imbedded  in  a white  feldspar  substance.  Under  the  microscope 
this  feldspar  appears  to  be  mostly  altered  to  a brownish  saussurite,  in 
spite  of  which,  however,  traces  of  a stout  lath-shape  are  discernible. 
The  hornblende  is  much  altered  to  a fibrous  form.  It  frequently  has 
the  emerald  green  color  of  actinolite,  especially  around  the  outer  edge, 
where  it  is  always  darker  and  more  compact  than  at  the  center.  lime- 
nite,  accompanied  by  leucoxene,  is  abundant  in  the  rock,  though  absent 
in  the  two  last  mentioned  specimens.  It  will  be  noticed  that  this  rock 
approaches  much  more  nearly  than  the  others  to  the  diabase  type,  and 
yet  there  is  no  reason  to  believe  that  the  hornblende  is  paramorphic 
after  pyroxene.  Although  it  is  not  compact,  it  still  retains  its  twinning 
structure  as  one  of  its  most  common  features. 

A still  more  striking  example  of  idiomorphic,  lath-shaped  feldspar 
in  a diorite  (a  structure  which  Bosenbuscli  mentions  as  not  at  all  un- 
common in  rocks  of  this  class1),  is  to  be  found  in  No.  11831.  This  was 
obtained  on  the  line  between  sections  5 and  8,  just  east  of  Nos.  11828, 
11829,  above  described.  It  is  entered  in  the  field-notes  as  a coarse 
reddish  diorite  or  syenite,  having  long,  green  hornblende  crystals  im- 
bedded in  a red  feldspar.  On  account  of  its  unstriated  feldspar,  this 
rock  may  perhaps  be  even  more  properly  designated  as  an  amphibole 
granite,  although  its  structure  is  in  many  respects  jieculiar.  (See  PI. 
XVI,  fig.  2.)  The  feldspar  is  present  in  two  distinct  generations. 
The  earliest  of  these  yielded  stoutly  lath-shaped  crystals,  which  are 
wholly  idiomorphic.  These  are  mostly  unstriated,  but  have  a zonal 
structure.  They  are  internally  changed  to  a grayish  mass,  which  a 


1 Mikros.  Physio#.,  2d  ed.,  vol.  2,  p.  121. 


182 


GREENSTONE  SCHIST  AREAS  OF  MICHIGAN. 


[ HULL.  62. 


high  magnifying  power  shows  to  be  muscovite  or  kaolin,  while  their 
periphery  is  composed  of  clear  and  fresh  feldspar  substance.  Between 
these  feldspar  crystals  is  a granular  aggregate  of  quartz  and  a younger 
feldspar.  This  latter  mineral  is  also  unstriated  (though  sometimes 
possessed  of  the  gridiron  microcline  structure)  and  much  fresher  than 
the  older  feldspar.  With  the  quartz  it  frequently  forms  beautiful 
micropegmatitic  growths. 

Hornblende  was  most  probably  the  original  bisilicate  constituent  of 
this  rock,  but  it  has  undergone  an  unusual  alteration,  i.  e.,  the  altera- 
tion to  mica.  This  mineral  can  be  seen  under  the  microscope  in  brown 
areas  of  irregular  shape,  which  have  evidently  been  produced  at  the 
expense  of  the  hornblende.1  They  are  unevenly  colored,  being  a 
darker  brown  in  some  places  than  in  others.  In  some  cases  the  new 
mica  crystallizes  in  sharply  defined  hexagonal  plates.  Certain  of  these, 
which  on  optical  examination  prove  to  be  basal  sections,  show  cleav- 
age lines  parallel  to  the  prismatic  faces.  These  are  the  so-called 
pressure  figures  (“Drucklinien”  of  the  German  mineralogists),  which 
are  rarely  visible  in  microscopical  sections  and  are  strongly  indicative 
of  pressure. 

This  secondary  mica  to  a considerable  extent  has  turned  green  by  a 
reduction  of  its  iron  to  a ferrous  state.  More  rarely  the  alteration  has 
progressed  still  further,  resulting  in  complete  bleaching,  or  even  the 
production  of  chlorite.  Apatite  is  very  abundant  in  this  rock;  sphene 
is  also  common,  but  its  crystals  always  surround  ilmenite  grains  in 
such  a manner  as  to  suggest  that  the  titanite  has  resulted  from  its 
alteration  (see  PI.  XVI,  fig.  2).  Chlorite  also  frequently  surrounds 
the  opaque  iron  mineral. 

Of  all  the  remarkable  features  which  this  rock  presents,  perhaps 
none  is  more  striking  than  its  hypidiomorphic  structure  and  the 
presence  of  the  feldspar  in  two  distinct  generations  without  the  pro- 
duction thereby  of  a porphyritic  structure.  This  is  all  the  more  note- 
worthy in  a rock  which  from  its  mineralogical  composition  is  to  be 
strictly  classed  among  the  granites. 

Xo.  11832,  which  occurs  with  the  specimen  last  described,  appears 
to  the  unaided  eye  as  a compact,  fine  grained  mass  through  which 
large  glistening  hornblende  crystals  are  unevenly  distributed.  Under 
the  microscope  the  groundmass  of  this  rock  is  seen  to  be  composed  of 
lath-shaped  feldspar  crystals,  which  are  altered  sometimes  to  epidote, 
sometimes  to  sericite;  allotriomorphic  hornblende,  frequently  changed 
to  chlorite;  a little  quartz  and  magnetite  in  grains  and  crystals. 
The  sharp  quadratic  and  hexagonal  sections  are  sufficient  to  iden- 
tify this  species;  but  we  must  assume  that  it  is  a titaniferous 
magnetite  on  account  of  the  very  narrow  leucoxene  border  which 


^osenbusch  mentions  only  parallel  growths  of  hornblende  and  biotite.  The  present  instance  can 
hardly  bo  so  interpreted,  while  there  is  nothing  surprising  in  an  alteration  which  has  been  so  fre- 
quently observed.  (Cf.  J.  Roth:  Allgemeine  und  chemische  Geologie,  vol.  1,  p.  333,  1879.) 


WILLIAMS.] 


DIABASES  OF  THE  NORTHERN  AREA. 


183 


frequently  surrounds  it.  The  porphyritic  hornblende  of  this  rock  is 
sometimes  regular,  sometimes  irregular  in  outline.  It  is  a later  crys- 
tallization than  the  groundmass,  because  it  is  always  filled  with  the 
lath-shaped  feldspars.  This  produces  the  structure  which  I have 
recently  termed  “poicilitic,”1  and  which  is  characteristic  of  younger 
porphyritic  crystals,  especially  hornblende  and  pyroxene. 

No.  11834,  from  a ledge  640  steps  north  and  20  steps  west  of  the  south- 
west corner  of  Sec.  4,  T.  48  N.,  K.  26  W.,  is  composed  of  stout,  lath-shaped 
feldspar  crystals  and  large  individuals  of  fibrous  hornblende.  The  for- 
mer mineral  suggests  by  its  form  that  the  rock  was  once  a diabase;  the 
hornblende,  however,  is  not  allotriomorphic,  but  is  present  in  long,  col- 
umnar crystals,  which  are  generally  twinned.  One  of  these  crystals  is 
bent  in  the  most  unaccountable  manner.  It  forms  three-quarters  of  a 
circle  (see  Fig.  28),  but  no  satisfactory  explanation  can  be  offered  for 
this  unusual  shape. 

On  the  whole,  this  rock  is  consid- 
erably altered.  Epidote  and  horn- 
blende needles  are  developed  in  its 
feldspar,  while  secondary  quartz  is 
quite  abundant.  In  spite  of  the 
fibrous  character  of  its  hornblende, 
the  structure  of  this  rock  is  much 
more  suggestive  of  a diorite  than  of 
a diabase. 

Diabase . — Among  the  altered  in- 
trusive rocks,  those  which  represent 
the  diabase  type  are  all  uralite  dia- 
bases. In  none  was  any  trace  of  the 
original  augite  observed. 

In  No.  11827,  from  485  steps  west  of  the  southeast  corner  of  Section 
5,  the  structure  is  best  preserved.  Here  the  fibrous  and  in  part  bright 
emerald  green  hornblende  retains  exactly  the  allotriomorphic  form  of 
the  diabase  augite.  The  feldspar  is  largely  altered  to  a brown,  opaque 
saussurite,  and  leucoxene  has  replaced  the  ilmenite. 

No.  11337,  from  815  steps  north  of  the  southwest  corner  of  Section 
4;  No.  11848,  from  500  steps  west  of  the  southeast  corner  of  Sec.  10, 
T.  48  N.,  K.  26  W.,  are  both  much  more  altered  than  the  specimen  last 
mentioned.  The  ophitic  structure  is  best  preserved  in  the  latter, 
although  epidote  is  abundantly  developed,  while  it  is  altogether  want- 
ing in  the  former. 

Other  of  these  uralite  diabases  are  finer  grained. 

No,  1 1825,  from  a somewhat  schistose  greenstone  ridge,  exposed  near 
the  center  of  the  southwest  quarter  of  Section  10,  admirably  exhibits 
the  effects  of  crushing.  The  lath-shaped  plagioclase  crystals  are  still 


Fig.  28.— Bent  hornblende  crystal.  Green- 
stone No.  11834.  Magnified  30  diameters. 


1 Am.  Jour.  Sci.,  3d  series,  vol.  31,  1886,  p.  30. 


184 


GREENSTONE  SCHIST  AREAS  OF  MICHIGAN. 


wonderfully  fresh,  but  are  broken,  faulted,  and  pulled  apart,  while  their 
interstices  are  filled  with  the  secondary  chlorite  usual  in  stretched 
rocks.  There  is  a delicate  granophyre  or  micropegmatite  structure  in 
this  specimen — undoubtedly  an  original  feature,  as  in  No.  11675  (see 
p.  140).  The  pyroxene  is  wholly  changed  to  a pale  green,  fibrous  horn, 
blende,  which,  to  a considerable  degree,  produces  the  foliation.  Large 
areas  of  brown  leucoxene,  of  the  variety  most  characteristic  of  altered 
diabase,  are  also  drawn  out  in  the  direction  of  the  schistose  structure. 
In  one  instance  this  has  altered  to  a network  of  dark  rutile  needles 
imbedded  in  a yellowish  micaceous  mineral,  as  described  in  No.  11070 
(see  p.  99,  and  Plate  XIII,  fig.  2). 

No.  11830,  from  700  hundred  steps  west  of  the  southeast  corner  of 
section  5,  is  a very  typical  uralite  diabase.  The  structure  is  still  well 
preserved  by  the  feldspars,  in  spite  of  needles  of  the  fibrous  hornblende 
having  freely  wandered  into  them.  Traces  of  augite  cores  remain  in 
this  rock. 

No.  11835  is  a schistose  rock  from  640  steps  north  and  20  west  of  the 
southeast  corner  of  Section  5.  It  has  been  much  altered,  and  now  con- 
sists mainly  of  a fine  aggregate  of  fibrous  hornblende,  feldspar,  quartz 
and  calcite.  In  this  lie  large  porphyritic  crystals  of  hornblende  which 
are  wholly  altered,  especially  in  their  interior. 

BANDED  GREENSTONES. 

Striped  and  banded  greenstone  schists,  like  those  of  Lighthouse  Point, 
Marquette,  are  very  abundant  in  the  northern  area. 

No.  11856,  from  an  exposure  near  the  northeast  corner  of  Section  9,  is 
macroscopically  identical  with  the  Marquette  rocks.  Under  the  micro- 
scope it  would  be  designated  as  a hornblende  schist.  It  consists  of  mi- 
nute crystalloids  of  compact  green  hornblende,  together  with  feldspar 
which  is  mostly  changed  to  sericite.  Zoisite  in  crystalloids,  like  those 
represented  in  Fig.  2,  p.  27,  and  about  the  size  of  the  hornblende,  is 
also  present.  The  structure  of  this  rock  is  schistose,  caused  by  the 
parallel  arrangement  of  all  the  constituents. 

Other  banded  greenstones  from  this  region,  like  No.  11818,  from  near 
the  southeast  corner  of  Section  5 $ 11821,  850  steps  north  of  the  south- 
west corner  of  Section  4;  11839,  170  steps  south  of  west  quarter  post  of 
section  4,  and  11841,  180  steps  north  of  the  same  quarter  post,  are 
essentially  like  the  specimen  just  described — mostly  a mass  of  con- 
fused hornblende  fibers  with  more  or  less  feldspathic  substance,  quartz, 
and  chlorite.  The  relative  proportions  of  these  components  condition 
their  different  colors  and  cause  the  parallel  striping. 

These  rocks  are  so  similar  to  those  occurring  immediately  north  of 
Marquette,  that  we  must  apply  to  them  the  conclusion  already  ex- 
pressed (p.  158)  in  regard  to  the  origin  of  these  green  schists,  and  regard 
them  as  basic  tuff  deposits,  which  were  contemporaneous  with  surface 
flows  of  diabase  and  subsequently  profoundly  metamorphosed. 


williams.]  FIELD  RELATIONS  OF  THE  DEER  LAKE  ROCKS.  185 

GREEN  SCHISTS  AND  AGGLOMERATES  OF  DEER  LAKE. 

After  the  work  on  this  paper  was  practically  completed,  my  atten- 
tion was  called  by  Prof.  Irving  to  a group  of  greenstone  schists  and 
conglomeratic  rocks  which  lie  in  the  western  extension  of  the  southern 
branch  of  Ihe  Marquette  greenstone-schist  belt.  I was  unable  to  study 
and  collect  these  rocks  in  the  field,  but  Prof.  Irving  furnished  me 
with  notes  regarding  their  distribution  and  mode  of  occurrence,  together 
with  a suite  of  hand-specimens  and  thin  sections  for  laboratory  study. 
I incorporate  the  results  of  such  a study  in  this  place  the  more  will- 
ingly because  the  occurrence  of  these  rocks  does  not  in  the  least  differ 
from  that  of  others  closely  allied  to  them,  which  I carefully  exam- 
ined in  the  neighborhood  of  Negaunee.  Tbe  distinct  evidence,  more- 
over, which  these  rocks  afford  as  to  their  mode  of  origin  is  of  great 
value  in  confirming  the  conclusions  already  reached  in  regard  to  cer- 
tain other  analogous,  though  less  distinctly  characterized,  occurrences. 

These  peculiar  rocks  are  best  exposed  on  the  south  side  of  Deer  Lake 
in  Secs.  33  and  34,  T.  48  2L,  R.  27  W.,  Michigan,  but  they  may  also  be 
advantageously  seen  farther  to  the  northwest,  in  Secs.  20,  21,  29,  and  30 
of  the  same  township. 

The  following  field-notes  were  furnished  me  by  Prof.  Irving : 

On  the  road  going  northward  from  Ishpeming  to  Deer  Lake  furnace  a belt  of 
quartzite  dipping  southward  is  crossed  in  the  middle  of  Section  34.  Immediately 
north  of  this  quartzite  follows  a porphyritic  greenstone  of  tolerably  fresh  aspect. 
This  is  exposed  on  the  south  side  of  the  two  knobs,  which,  on  Dr.  Rominger’s  map, 
lie  to  the  southward  of  Deer  Lake,  to  the  east  of  the  Carp  River,  and  to  the  north  of 
the  road.  To  the  northward  of  this  greenstone  succeed  first  some  greenish  schistose 
rocks  without  apparent  agglomeratic  character.  These  are  represented  by  No.  12057. 
These  schists  soon  grade,  however,  both  across  the  strike  toward  the  north  and  in 
the  course  of  the  strike  toward  the  west,  into  a most  strikingly  conglomeratic  rock, 
which  appears  to  make  up  about  all  the  hills  in  the  northern  half  of  Section  33,  be- 
tween the  quartzite  and  the  road  leading  to  the  Ropes  mine. 

Specimen  No.  12058  is  an  obscurely  conglomeratic  rock,  collected  about  150  steps 
north  of  No.  12057.  The  conglomeratic  character  is  best  seen  on  a weathered  sur- 
face. A particularly  fine  exposure  may  be  seen  just  west  of  Deer  Lake  furnace 
(No.  12031). 

Specimens  No.  12029  are  pebbles  from  a hold  knob  somewhat  farther  to  the  west. 
From  the  same  point  came  Nos.  12023  and  12024,  representing  the  conglomerate 
itself ; and  Nos.  12025  and  12026,  from  two  dikes  two  and  one-half  and  ten  feet  wide 
respectively.  The  smaller  of  these  dikes  cuts  the  conglomerate  in  a direction  trans- 
verse to  its  foliation,  while  the  larger  runs  parallel  to  this  structure. 

Throughout  the  conglomerate  there  is  a tendency  to  schistose  structure,  which, 
however,  is  never  very  pronounced,  and  which  varies  considerably  in  its  degree  of 
development.  It  seems  to  be  rather  the  result  of  the  intersection  of  close  joints  cut- 
ting each  other  at  a small  angle  than  a true  parallelism  of  structure.  This  foliation 
stai  ds  about  vertical  and  trends  in  an  eastern  and  western  direction. 

The  pebbles  vary  in  size  from  such  as  are  two  feet  in  diameter  down  to  minute 
fragments.  Pieces, less  than  six  inches  in  length  are  most  abundant.  Occasionally 
they  appear  well  rounded,  and  this  seems  to  be  more  particularly  tbe  case  with  tbe 
larger  sized  pieces  ; but  more  commonly  they  are  sub-angular  and  flattened  out  in  a 
direction  parallel  to  the  schistose  structure.  On  an  exposed  surface  these  pebbles 


186 


GREENSTONE  SCHIST  AREAS  OF  MICHIGAN. 


[BULL.  62. 


stand  out  by  virtue  of  tbeir  whiter  weathering.  On  a fresh  fracture  they  are  not 
nearly  so  apparent,  but  seem  to  differ  from  the  rest  of  the  rock  by  their  finer  grain 
and  by  their  pinkish  or  greenish  color ; the  body  of  the  rock  having  usually  a dark 
greenish  gray  tint. 

No  other  kinds  of  pebbles  were  seen  than  those  shown  in  the  samples,  which  repre- 
sent perhaps  two  phases : (1)  A pinkish  weathering  felsitic  (?)  kind,  and  (2)  a grayish 
weathering  greenish  and  more  schistose  kind.  But  this  distinction,  written  on  the 
ground,  seems  hardly  to  be  borne  out  by  the  specimens  brought  away.  Certainly 
those  of  the  first  named  kind  are  more  abundant. 

Occasional  schistose  bands  a few  feet  in  width  and  quite  free  from  pebbles  may  be 
seen  in  the  conglomerate,  trending  east  and  west.  These,  therefore,  stand  at  a con- 
siderable angle  with  the  schistose  structure.  They  are  the  only  signs  of  a true  bed- 
ding in  the  rock,  and  if  they  do  actually  indicate  a bedding  are  of  very  great  im- 
portance, both  as  showing  a discordance  between  the  bedding  and  schistosity  and 
also  a nonconformity  between  these  and  the  true  bedded  rocks  lying  just  to  the 
south.  Indeed,  neither  these  doubtful  bedding  bands  nor  the  schistose  structure 
perceptible  in  this  conglomerate  is  concordant  with  the  dip  ofthe  quartzite,  which 
is  toward  the  south  at  a moderate  angle. 

North  of  the  road  leading  to  the  Ropes  mine  the  only  rock  noticed,  for  a short 
distance,  is  represented  by  No.  12032,  which  does  not  show  any  conglomeratic  struct- 
ure, but  which  on  the  ground  appeared  very  much  like  the  pebbles  in  the  conglom- 
erate further  south. 

Still  farther  north,  in  the  same  township  (T.  48  N.,  R.  27  W.),  as,  for  instance,  in 
the  middle  and  eastern  part  of  Section  21,  and  again  in  the  southwest  quarter  of  Sec- 
tion ?0,  and  in  the  northwest  quarter  of  Section  29,  to  the  north  of  Dr.  Rominger’s 
serpentine  area  (peridotite  area  of  Plate  I,  herewith)  are  other  very  similar  rocks. 
Specimens  12036,  12037,  and  12039  are  from  the  SW  £ of  SYV  £ Sec.  20,  while  No.  12043 
is  from  the  NW  \ Sec.  29.  Among  the  exposures  from  which  this  last  specimen 
was  taken  are  some  which  seem  to  show  the  conglomeratic  character  of  the  Deer 
Lake  rocks.  It  is  not  positive,  however,  that  the  obscure  markings  which  they 
show  are  really  those  of  pebbles. 

Both  the  macroscopical  and  the  microscopical  examination  of  these 
specimens  show  that  they  have  been  subjected  to  an  intense  strain  or 
stretching,  which  has  resulted  in  the  elongation  of  the  component  peb- 
bles, and  in  the  modification  and  partial  recrystallization  of  the  matrix, 
after  the  manner  shown  in  PI.  XI,  fig.  2,  and  in  PI.  XIV,  fig.  2.  Nev- 
ertheless, the  metamorphism  attendant  upon  this  dynamic  action  fortu- 
nately has  not  been  sufficient  entirely  to  disguise  the  tuff  nature  of  the 
rock.  In  most  cases  this  is  still  very  apparent,  and  this  occurrence  is 
therefore  of  great  importance  in  confirming  the  conclusions  reached  with 
regard  to  analogous,  but  more  metamorphosed  rocks,  in  the  Marquette 
and  Negaunee  areas. 

We  must  regard  these  tuffs  or  agglomerates  as  originally  composed 
of  the  fine  fragmental  material  of  diabase.  This  consisted  mainly  of 
triclinic  feldspar  and  pyroxene,  mingled  with  more  or  less  amorphous 
base,  and  stratified  either  by  gravity  or  by  the  agency  of  water.  In- 
cluded in  such  a matrix  were  numerous  true  bombs  of  solid  diabase  and 
ejected  fragments  of  other  rocks,  mostly  of  a more  acid  character. 

As  is  well  known,  material  of  this  kind  is  of  all  the  most  liable  to  un- 
dergo chemical  alteration.  This  has  been  conclusively  shown  by  the 
observations  of  Captain  Dutton,  quoted  above  (p.  159).  In  consideration 


*\r: S i ■ 

■ " willums.  1 AGGLOMERATES  OF  DEER  LAKE.  187 

of  the  great  antiquity  of  the  deposits  here  under  discussion,  therefore  it 
need  excite  no  wonder  that  little  of  the  original  material  now  remains. 
The  rocks  are  largely  composed  of  such  secondary  products  as  chlorite, 
sericite,  epidote,  quartz,  and  calcite.  All  traces  of  original  pyroxene, 
or  of  possible  olivine  and  glass,  have  wholly  disappeared.  The  feldspar 
* has,  however,  better  retained  its  individuality.  In  some  instances  its 
substance  is  still  quite  fresh ; and  in  others,  where  the  substance  is 
changed,  the  form  is  still  easily  recognizable.  The  same  class  of  altera- 
tions has  gone  on  in  the  solid  portions  of  the  agglomerates  as  in  the 
finely  fragmental  matrix.  The  more  basic  fragments  produce  chloritic, 
the  more  acid  sericitic,  areas.  Their  original  boundaries  are,  however, 
for  the  most  part,  very  distinct,  often  more  so  in  the  field,  or  in  the 
hand-specimen,  than  under  the  microscope.  Where  the  dynamic  action 
has  been  most  intense  a schistose  structure  has  been  developed  in  the 
fragments,  which  is  quite  continuous  with  that  of  the  finer  grained  ma- 
trix. This  is  accompanied  by  a distortion  or  elongation  of  the  in- 
cluded fragments,  caused  by  crushing  and  recementing,  whereby  the 
sharpness  of  their  outline  is  destroyed,  and  an  apparent  transition  to 
the  matrix  is  produced. 

Specimen  No.  12057,  described  in  the  notes  as  “a  greenish  schistose 
rock  without  apparent  agglomeratic  character,” appears  under  the  micro- 
scope at  first  glance  as  a confused  aggregate  of  chlorite,  calcite,  and 
quartz,  through  which  occasional  large  grains  of  yellowish  green 
epidote  are  scattered.  Characteristic  forms  of  ilmenite,  with  leucoxene, 
some  sericite,  and  delicate  little  rutile  needles  are  also  present.  A 
more  careful  study  of  this  section  reveals  the  indistinct  outlines  of  lath- 
shaped feldspars,  which  once  formed  the  interlacing  network  of  a 
granular  diabase.  These  are  so  disguised  by  the  new  products  devel- 
oped in  them — chlorite,  sericite,  and  epidote — that  it  is  only  by  an 
attentive  examination  with  a low  magnifying  power  that  they  can  be 
recognized.  They  are,  however,  undoubtedly  present,  and  the  rock 
must  therefore  be  regarded,  not  as  a tuff,  but  as  an  extremely  metamor- 
phosed form  of  a massive  flow,  in  which  the  profound  chemical  changes 
and  the  development  of  a schistose  structure  progressed  together. 

Specimen  No.  12058,  “an  obscurely  conglomeratic  rock  collected 
about  150  steps  north  of  the  locality  of  No.  12057,”  bears  in  the  hand- 
specimen  a close  resemblance  to  the  one  last  described,  but  under  the 
microscope  its  different  character  is  at  once  apparent.  The  feldspar 
substance  is  here  less  altered,  and  the  rock  is  mostly  composed  of 
minute  crystals  or  fragments  of  crystals  connected  by  that  peculiar 
aggregate  of  chlorite  scales  common  in  stretched  basic  rocks,  where  the 
direction  of  the  scales  follows  the  schistose  structure.  (See  PI.  XI, 
fig.  2.)  Occasional  larger  fragments  of  feldspar  crystals  are  scattered 
through  this  finer  mass,  but  these  are  always  broken  and  irregular  in 
shape.  The  chloritic  substance  has  doubtless  originated  from  the  py- 
roxene or  glass,  while  a vast  number  of  the  most  delicate  little  rutile 


188 


GREENSTONE  SCHIST  AREAS  OF  MICHIGAN. 


[BULL.  62. 


needles,  arranged  in  long,  sinuous  bands,  appears  to  represent  the 
original  ilmenite.  Calcite  areas  also  occur.  A narrow  white  vein 
which  traverses  this  hand-specimen  possesses  an  interesting  micro- 
scopic structure.  The  little  fissure  was  first  coated  with  chalcedonic 
quartz,  and  then  with  a layer  of  quartz  crystals  which  projected  their 
terminations  into  the  opening.  These  possess  a perfect  zonal  structure, 
due  to  the  arrangement  in  successive  layers  of  fluid  inclusions.  The 
remainder  of  the  space  was  subsequently  filled  with  carbonate. 

Specimen  No.  12031,  from  a point  a short  distance  west  of  where  the 
last  mentioned  pieces  were  collected,  and  Nos.  12023,  12024,  32029,  and 
12030,  from  another  point  still  farther  west,  represent  the  agglomerate 
in  its  most  typical  development,  and  leave  no  doubt  as  to  its  true 
nature  and  origin.  As  in  the  specimens  last  mentioned,  the  matrix  of 
the  rock  is  of  a grayish  green  color  and  the  grain  is  mostly  aphanitic, 
although  frequent  minute  angular  fragments  may  be  detected  by  the 
aid  of  a pocket  lens.  There  is  always  a more  or  less  pronounced  folia- 
tion developed  in  this  matrix.  The  pebbles,  which  impart  to  the  rock 
its  agglomeratic  structure,  show  most  distinctly  on  a weathered  sur- 
face. Here  they  present  a white  or  pinkish  gray  color,  which  contrasts 
most  sharply  with  the  pale  green  of  the  inclosing  matrix.  On  a fresh 
fracture  the  inclusions  have  a greenish  gray  color,  but  their  compact, 
fine  grain,  like^  that  of  halleflinta,  serves  to  identify  them  where  the 
color  fails.  These  massive  felsitic  fragments  are  of  varying  size  and 
angular  or  subangular  in  shape  (rarely  well  rounded).  They  are  dis- 
tributed through  the  matrix  indiscriminately,  the  longest  axes  being  by 
no  means  parallel,  as  we  might  expect  in  a sediment.  The  foliation  of 
the  rock  appears  to  have  been  produced  by  a great  tension,  which  has 
stretched  the  matrix  and  sometimes  elongated  the  pebbles,  sometimes 
broken  them,  and  sometimes  forcibly  torn  the  solidified  matrix  away 
from  them.  The  latter  case  is  represented  in  Fig.  29,  which  represents 


Fig.  29.— Weathered  surface  of  a specimen  of  the  Deer  Lake  agglomerate. 
Natural  size.  No.  12023. 


the  appearance  of  a weathered  surface  on  specimen  No.  12023.  It  can 
here  be  plainly  seen  that  the  longest  axes  of  the  pebbles  stand  almost 
at  right  angles  and  that  the  matrix  has  been  forcibly  separated  by  the 
stretching  action,  on  each  side  of  the  central  pebble. 


WILLIAMS.]  MASSIVE  DIABASE  OF  DEER  LAKE.  189 

The  microscopical  study  of  these  specimens  adds  much  to  our  knowl- 
edge of  the  true  structure  of  these  agglomeratic  rocks. 

The  matrix  is  found  to  be  composed  of  very  angular  to  subangular 
fragments,  extending  down  to  the  minutest  size.  These  generally  still 
retain  their  form,  although  their  original  substance  has  undergone 
change  to  chlorite,  epidote,  and  calcite.  Small  feldspar  crystals  or 
broken  fragments  of  larger  ones  are  scattered  about,  the  substance  of 
which  has  been  altered  in  varying  degree.  In  the  chlorite  especially, 
very  sharp  rutile  needles  abound.  These  seem  to  represent  the  titan- 
ium of  an  original  ilmenite. 

Unmistakable  evidence  of  clastic  structure  is  everywhere  encount- 
ered; but  this  is  not  the  clastic  structure  of  a sediment.  The  angular 
shape,  different  substance,  and  enormous  variation  in  the  size  of  frag- 
ments lying  side  by  side,  all  clearly  indicate  an  agglomeration  of  vol- 
canic detritus — and  one,  indeed,  in  which  many  of  the  original  features 
are  admirably  preserved. 

Among  the  smallest  of  the  included  fragments,  those  resembling  a 
massive  diabase  in  structure  are  not  uncommon;  but  to  judge  from 
the  statement  in  the  field  notes  quoted  above,  as  well  as  from  the 
hand-specimens  submitted  to  me  for  study,  the  larger  “pebbles”  or 
fragments  are  mostly  composed  of  the  lighter  and  felsitic  rock.  This  is 
unfortunately  too  much  altered  to  allow  of  a wholly  satisfactory  diag- 
nosis. It  may  be  best  seen  in  section  No.  12023,  where  it  resembles  a 
porphyrite.  The  grouudmass  still  retains  its  ophitic  structure,  and 
is  filled  with  well  formed  porphyritic  crystals  of  plagioclase.  No 
original  quartz  nor  orthoclase  could  be  detected  ; one  or  two  chloritic 
areas,  which  must  probably  represent  former  augite  or  hornblende 
crystals,  were,  however,  observed. 

Specimen  No.  12025  represents  a narrow,  transverse  dike  of  massive 
greenstone,  and  No.  12026  a broader  one  of  the  same  material,  parallel 
to  the  schistose  foliation.  Under  the  microscope  both  are  typical, 
though  highly  altered  diabases.  The  former  is  aphanitic  and  has 
only  a very  indistinct  foliation  in  the  hand-specimen.  Under  the 
microscope  the  original  structure  is  nearly  obliterated ; still,  traces  of 
it  remain.  Chlorite,  calcite,  quartz,  and  iron  oxide  are  almost  the  only 
mineral  components. 

The  second,  coarse  grained  diabase,  is  entirely  massive  in  the  hand- 
specimen.  It  has  an  even  green  color,  but  cleavage  surfaces  of  feld- 
spar are  frequent.  Pyrite  is  also  common  in  it.  Under  the  microscope 
the  typical  diabase  structure  is  perfectly  preserved.  The  texture  is 
quite  coarse,  and  the  feldspars  mostly  retain  their  twinning  structure. 
The  rock  has  been  stretched,  and  these  feldspars  are  much  broken  and 
have  their  fragments  separated.  The  pyroxene  is  wholly  altered  to 
chlorite,  epidote,  and  calcite,  and  the  ilmenite  is  accompanied  by 
leucoxene. 

The  rock  occurring  north  of  the  road  leading  to  the  Ropes  mine  and 


190 


GREENSTONE  SCHIST  AREAS  OF  MICHIGAN. 


[bull.  62. 


directly  west  of  Deer  Lake,  is  devoid  of  conglomeratic  structure. 
(No.  12032.)  In  the  field  it  was  noted  to  have  a resemblance  to  the 
substance  of  the  larger  “ pebbles,”  and  this  resemblance,  to  a certain 
extent,  is  borne  out  by  the- microscopical  examination.  The  rock  ap- 
pears to  be  massive,  and  not  a tuff;  but  it  has  been  subjected  to  in- 
tense crushing  and  stretching  action.  It  is  full  of  porphyritic  crystals, 
which  are  mostly  altered  to  muscovite.  The  groundmass  is  principally 
composed  of  small  rectangular  feldspar  crystals.  All,  however,  are 
much  broken  and  separated,  and  the  interstices  are  filled  with  green 
chlorite  scales.  The  main  difference  between  this  rock  and  that  form- 
ing the  compact  felsitic  pebbles  in  the  agglomerate  lies  in  the  apparent 
orthoclastic  nature  of  the  porphyritic  feldspar  crystals,  and  in  the 
chlorite  which  has  been  so  abundantly  developed  in  the  groundmass. 

The  specimens  from  the  more  northerly  areas,  numbered  12036, 
12037,  12030,  and  12043,  belong  to  the  same  category  as  those  just 
described.  No.  12036  is  a confused  aggregate  of  feldspar  fragments  of 
various  sizes,  together  with  some  quartz  and  chlorite.  Nos.  12039  and 
12043  are  almost  too  much  altered  to  allow  of  any  study.  The  former 
is  a mass  of  nearly  opaque  decomposition  products,  and  the  latter  is  an 
almost  continuous  mat  of  sericite  scales.  No.  12037  alone  appears  like 
a massive  rock— most  probably  a fragment  included  in  the  tuff.  It  is 
a hornblende  granite,  with  but  little  quartz,  composed  principally  of 
idiomorphic  feldspar.  The  minute  green  hornblende  needles  fill  the 
interstices  between  these  square  or  rectangular  crystals. 

We  may,  therefore,  consider  the  pyroclastic1  nature  of  the  Deer  Lake 
conglomerates  as  beyond  any  question.  They  represent  volcauic  de- 
tritus, ejected  by  an  explosive  force  at  the  earth’s  surface.  In  this  way 
they  form  a most  welcome  but  not  unexpected  support  to  the  con- 
clusions reached  in  regard  to  the  other  more  highly  altered  rocks  of 
the  same  class  occurring  in  the  Marquette  region. 

The  term  “agglomerate”  here  applied  to  these  rocks  is  one  in  gen- 
eral usage  among  the  English  geologists  2 to  designate  a tumultuous 
assemblage  of  volcanic  ejectamenta — bombs,  foreign  blocks,  etc.,  of  all 
sizes  and  shapes,  cemented  by  a fine  grained  paste  of  volcanic  ash. 

The  closest  analogues  to  the  Deer  Lake  rocks  are  the  breccias,  ag- 
glomerates, and  tuffs,  described  by  Dr.  A.  Geikie  from  St.  David’s,  in 
Wales.3  This  author  says,  p.  93: 

The  rocks  of  St.  David’s  present  features  of  interest  and  importance,  not  only  in 
the  palaeozoic  history  of  Britain,  but  in  regard  to  general  theoretical  questions. 
They  include,  for  example,  perhaps  the  oldest  group  of  lavas  and  tuffs,  the  relative 
date  of  which  is  known.  They  have  been  subjected  to  a process  of  metamorphism 
which  has  affected  only  certain  beds  or  kinds  of  rock.  They  have  been  penetrated 
by  masses  of  granite  and  quartz  porphyry,  around  which  another  kind  of  metainor- 
phism  has  been  manifested.  At  a later  period  they  have  been  injected  with  diabase 
dikes,  etc. 

1 J.  J.  H.  Teall,  Geol.  Mag.,  London,  3d  series,  vol.  4,  November,  1887,  p.  493. 

2Cf.  J A.  Phillips,  Quart.  Jour.  Geol.  Soc.,  vol.  24, 1878,  p.  476,  and  A.  Geikie  Text-Book  of  Geology, 
1882,  p.  163. 

2 Quart.  Jour.  Geol.  Soc.,  London,  vol.  39, 1883. 


Williams.]  AGGLOMERATES  OF  ST.  DAVID’S,  IN  WALES.  191 

All  this  might  have  been  written  to  apply  equally  well  to  the  rocks 
occurring  near  Marquette. 

With  special  reference  to  the  tuffs,  Dr.  Geikie  says  :l 

They  vary  likewise  in  texture  from  somewhat  coarse  breccias  or  agglomerates, 
through  many  gradations,  into  fine  silky  schists  in  which  the  tufaceous  character  is 
almost  lost.  Generally  they  are  distinctly  granular,  presenting  to  the  naked  eye 
abundant  angular  and  subanglar  lapilli,  among  which  broken  crystals  of  a white, 
somewhat  kaolinized  feldspar  and  fragments  of  fine  grained  felsite  are  often  con- 
spicuous. 

The  matrix  of  these  Welsh  agglomerates  appears  to  be  generally 
green,  while  the  included  lapilli  or  u pebbles”  are  sometimes  basic  in 
character  aud  of  a greenish  color  $ sometimes  more  acid,  with  a com- 
pact structure  and  pinkish  color. 

Their  resemblance  is  thus  seen  to  be  very  close  to  the  Deer  Lake 
agglomerates  described  in  this  chapter. 


Quart.  Jour.  Geol.  Soc.  London,  vol.  39,  p.  295. 


CHAPTER  VI. 


GENERAL  RESULTS  AND  CONCLUSIONS. 

ORIGINAL  CHARACTER  OF  THE  MENOMINEE  AND  MARQUETTE  GREEN- 
STONE AREAS. 


In  speaking  of  the  geology  of  the  Menominee  and  Marquette  regions 
I refer,  it  must  be  understood,  only  to  the  greenstones  and  certain  inti- 
mately associated  acid  rocks.  Ho  attention  was  paid  to  the  quartz- 
ites, dolomites  or  shales  of  the  younger,  iron-bearing  Huronian.  With 
a view  of  obtaining  a clear  idea  of  the  primary  nature  of  these  rocks 
we  shall  consider  in  succession : The  evidence  of  their  eruptive  charac- 
ter; their  original  types  and  mineralogical  composition;  the  conditions 
under  which  they  were  formed;  and,  finally,  their  succession  in  time. 


EVIDENCE  OF  ERUPTIVE  CHARACTER. 


Field  evidence. — This  is  more  distinct  in  the  case  of  the  Menominee 
greenstones  on  account  of  the  simpler  character  of  their  exposures. 
Here  we  find  them  extending  in  two  comparatively  narrow  and  nearly 
parallel  bands  for  a considerable  distance.  Their  color,  weight,  text- 
ure, and  frequent  massive  structure  are  such  as  are  associated  with  rocks 
of  igneous  origin,  while  in  some  cases,  as  just  below  the  Lower  Quinne- 
sec  Falls,  they  project  out  of  the  surrounding  schists  in  the  form  of  a 
high,  precipitous  ridge,  suggestive  only  of  a great  dike.  Although 
successive  layers  of  these  rocks  differ  considerably  in  composition,  and 
though  they  possess  within  themselves  well  marked  schistose  varieties, 
yet  they  are  sharply  defined  against  the  adjoining  Huronian  beds,  into 
which  they  never  pass  by  gradual  transitions.  Indeed,  these  rocks  have 
been  considered  by  many  of  the  geologists  who  have  examined  them 
most  carefulty  as  of  eruptive  origin.  Those,  on  the  other  hand,  who 
have  regarded  them  as  either  wholly  or  partially  sedimentary  have 
been  able,  as  far  as  I know,  to  cite  only  two  arguments  in  favor  of  their 
opinion.  These  are : First,  the  coincidence  of  the  direction  of  these 
bands,  and  of  their  alternating  component  members  with  the  general 
strike  of  all  the  rocks  of  this  region ; and,  second,  the  frequent  con- 
formity of  the  schistose  structure  in  these  bands  to  the  bedding  of  the 
adjacent  sediments.1 

Let  us,  however,  consider  whether  these  two  facts  are  not  wholly  in 
accord  with  the  supposition  that  these  greenstones  are  of  igneous  origin. 


This  conformity  is  by  no  moans  universal. 


11)2 


WILLIAMS. ) 


EVIDENCE  OF  ERUPTIVE  CHARACTER. 


193 


If  they  were  intrusive  they  would  follow  in  their  course  the  line  of  least 
resistance,  which  would  probably  be  the  direction  of  the  bedding  of  the 
sediments.  If,  however,  as  seems  from  various  considerations  much 
more  probable,  these  greenstones  belong  to  a formation  older  than  the 
Huronian,  and  if  they  were  produced  in  the  form  of  great  igneous  (and 
perhaps  submarine)  overflows  which  composed  the  bottom  of  the  basin 
in  which  the  iron-bearing  sediments  were  subsequently  deposited,  then 
the  great  lateral  compression,  which  so  contorted  these  sediments  and 
elevated  them  into  their  present  almost  vertical  position,  would  have 
brought  the  underlying  greenstones  at  the  same  time  into  just  the  posi- 
tion they  now  occupy.  And  if  these  greenstones  had  been  formed  as 
successive  flows,  differing  more  or  less  in  structure  and  composition,  in 
the  process  of  upheaval  they  must  have  behaved  like  any  other  com- 
plex of  horizontal  beds  and  have  produced  conformable  members  of  the 
series  exposed  in  the  Menominee  valley,  as  is  actually  the  case. 

Now,  also  in  regard  to  the  second  point  of  objection,  if  we  admit  that 
massive  rocks  may  have  a schistose  structure  (like  a slaty  cleavage), 
developed  in  them  by  pressure,  then,  in  this  case,  the  direction  of  this 
cleavage,  perpendicular  to  the  action  of  the  pressure,  must  agree  with 
the  stratification  of  the  now  almost  vertical  sediments. 

Nor  is  it  necessary  to  assume  that  the  schistosity  of  these  rocks  was 
wholly  produced  at  the  same  time  with  the  crumpling  and  slaty  cleav- 
ages of  the  overlying  detritals;  since  the  same  crumpling  force  may 
have  worked  in  the  same  direction  at  two  widely  separated  periods. 
Indeed,  there  is  excellent  reason  to  believe  in  two  such  periods,  since 
the  dikes,  which  in  the  Marquette  region  penetrated  the  greenstone 
schists  subsequent  to  their  being  made  schistose,  have  evidently  them- 
selves been  subjected  to  further  squeezing.  These  dikes  appear  to  be 
contemporaneous  with  the  sheets  of  greenstone  interfolded  with  the 
detrital  iron-bearing  strata,  which  sheets  themselves  show  a similar  de- 
gree of  schistosity  with  the  dikes  referred  to.  In  the  Marquette  region 
there  is  generally  a very  noticeable  difference  as  to  the  amounts  of  sec- 
ondary cleavage  in  the  greenstone  schist  area,  and  in  the  strata  of  the 
overlying  iron-bearing  series,  this  being  very  much  greater  in  the  former 
case.  Coincident  with  this  difference  is  the  frequent  gentle  bowing  of 
the  iron-bearing  strata  in  this  region,  the  dips  of  its  layers  being  often 
quite  flat,  while  the  cleavage  of  the  green  schists  always  stands  at  a 
very  high  angle.  In  the  Menominee  region,  on  the  other  hand,  the 
folding  of  the  iron-bearing  series  is  very  much  closer  and  slaty  cleavage 
is  much  more  generally  developed.  This  would  seem  to  indicate  that 
the  second  period  of  squeezing  was  more  intense  in  the  Menominee 
area,  and  that  it  was,  therefore,  probably  more  instrumental  in  render- 
ing the  greenstones  schistose  here  than  in  the  Marquette  region. 

The  arguments  used  by  the  defenders  of  the  sedimentary  origin  of 
the  Menominee  greenstones  can  not  therefore  be  regarded  as  valid. 

On  the  other  hand  we  may  cite,  as  positive  evidence  that  the  foliation 
Bull.  62 13 


194 


GREENSTONE  SCHIST  AREAS  OF  MICHIGAN. 


I BULL.  62. 


of  the  greenstones  is  a secondary  feature,  the  fact  stated  by  Major 
Brooks,  that  at  the  Four-Foot  Fall  this  foliation  is  conformable  to  the 
adjoining  clay-slate,  which  has  a “ stroug  cleavage  and  no  distinguish- 
able bedding  planes.”1  Thus  the  schistose  structure  of  the  greenstone 
now  agrees  with  the  secondary  slaty-cleavage  of  the  sediment,  which, 
of  course,  may  or  may  not  agree  with  its  original  bedding,  since  this 
is  here  obliterated.  Furthermore,  what  foliation  the  greenstones  pos- 
sess may  be  traced  in  almost  every  case  into  a jointing,  or  into  bands 
produced  by  the  crushing  attendant  upon  faulting  and  slipping,  which 
has  taken  place  within  the  rock-mass.  Finally,  the  abruptness  with 
which  the  foliation  of  the  greenstones  commences  and  breaks  off  in  the 
direction  of  the  strike  is  wholly  inconsistent  witlr  the  theory  that  it  is 
due  to  original  stratification.  At  the  Four-Foot  Fall,  for  instance,  the 
greenstones  strike  almost  at  right  angles  to  the  river,  and  yet  they  are 
very  schistose  on  the  Wisconsin  and  very  massive  on  the  Michigan 
bank.  Such  cases  are  not  uncommon  while  even  more  difficult  to  ex- 
plain are  differences  in  the  strike  of  schistose  bands  which  traverse 
a massive  rock  (like  those  observed  at  the  Upper  Twin  Fall),  unless  we 
assume  that  they  were  produced  by  a force  which  acted  unevenly  and 
not  in  a constant  direction. 

The  field  evidence  that  the  greenstones  within  the  Marquette  belt 
are  of  igneous  origin  is  not  so  plain  as  that  encountered  in  the  Menom- 
inee valley.  Although  we  find  here  unmistakable  dikes  of  unal- 
tered diabase  and  others  of  altered  though  still  massive  greenstone, 
yet  some  of  the  most  important  of  these  rocks,  especially  in  the  north- 
ern part  of  the  Marquette  area,  are  so  regularly  banded  and  stratified 
that  we  are  obliged  to  seek  the  agency  of  water  to  account  for  their 
formation.  Nevertheless,  we  are  not  obliged  to  separate  even  these 
greenstones  altogether  from  the  igneous  rocks  which  accompany  them. 
For  reasons  stated  at  length  in  Chapter  IV,  they  may  be  most  satis- 
factorily explained  as  tuff  deposits,  half  volcanic,  half  sedimentary, 
which  throw  important  light  upon  the  physical  conditions  under  which 
the  more  massive  rocks  were  produced. 

Strong  collateral  evidence  respecting  the  original  nature  of  the  green- 
stones of  both  these  areas  may  be  obtained  from  a study  of  the  acid  rocks 
which  are  quite  constantly  associated  with  them.  The  indications  of 
the  eruptive  character  of  these  rocks  are  so  unmistakable  that  it  seems 
to  have  hardly  ever  been  doubted  by  any  one  who  has  examined  them. 
Large  areas  of  granite  occur  on  each  side  of  the  Huronian  basins,  both 
in  the  Menominee  valley  and  near  Marquette,  and  dikes  and  apophyses, 
presumably  radiating  from  these  main  masses,  penetrate  the  green- 
stones for  a considerable  distance  (cf.  the  Upper  Quinnesec  Fall,  Horse 
Eace,  and  region  just  north  of  Marquette).  How,  the  composition  of 
these  acid  rocks  is  such  that  they  resist  chemical  alteration  much  more 
successfully  than  those  of  a more  basic  character.  Hence  we  should 


‘■Geol.  Wisconsin,  vol.  3,  p.  475. 


williams.]  FIELD  EVIDENCE  OF  ERUPTIVE  CHARACTER. 


195 


expect  to  find  their  distinctively  eruptive  features,  such  as  dike-form, 
line  of  contact,  original  structure,  etc.,  much  better  preserved.  This  is 
the  case,  and  yet  these  eruptive  rocks  often  present  phenomena  of  sec- 
ondary foliation  quite  identical  with  those  seen  in  the  greenstones. 

Near  the  southern  end  of  the  Brook  Section,  just  west  of  Marquette, 
this  intrusive  granite  is  filled  with  fragments  of  the  surrounding  schist 
which  it  tore  off  while  yet  in  a molten  state.  At  the  lower  end  of  the 
Horse  Race  Rapid,  on  the  Menominee  River,  the  acid  dikes  show  a 
marked  diminution  in  the  size  of  the  grain  toward  the  dike  walls,  a 
structure  eminently  characteristic  of  rocks  which  have  crystallized  in 
fissures.  Near  Upper  Quinnesec  Falls  also  was  discovered  a rock  closely 
resembling  a granitic  hornfels  (No.  11064).  But  in  spite  of  all  the  evi- 
dence that  the  acid  rocks  are  eruptive,  their  dikes,  for  the  most  part, 
follow  the  strike  of  those  through  which  they  break,  since  this  is  the 
line  of  least  resistance,  while  many  of  them  have  a perfect  foliation  and 
even  a gneissic  structure.  What  we  may  regard  as  satisfactory  proof 
that  this  foliation  is  a secondary  feature  may  be  seen  at  the  head  of  the 
Horse  Race,  where  it  conforms  to  the  general  strike  of  the  surrounding 
greenstones,  even  where  this  does  not  coincide,  as  is  exceptionally  the 
case,  with  the  sides  of  the  acid  band  (see  p.  115).  A similar  structure 
has  been  observed  by  Prof.  Oh.  E.  Weiss,  of  Berlin,  near  Thai,  in  Thu- 
ringia and,  like  the  present  case,  it  may  be  regarded  as  certain  evi- 
dence that  a schistose  or  even  A banded  structure  may  be  developed  in 
acid  dikes  by  secondary  causes,  independent  of  their  own  direction, 
but  conformable  with  the  strike  of  the  surrounding  rocks. 

Microscopical  evidence. — The  most  convincing  proof  that  the  rocks  of 
the  Menominee  aud  Marquette  greenstone  areas  are  of  igneous  origin 
is  not  to  be  derived,  however,  from  their  field  relations,  but  rather  from 
their  microscopical  structure.  It  is  true  that  there  are  many  cases 
where  rocks  of  widely  dissimilar  origin  resemble  one  another  so  closely 
that  not  even  the  minutest  study  of  their  internal  structure  is  able  to 
distinguish  them  with  certainty  ; nevertheless  there  are  in  other  cases 
well  marked  peculiarities  of  structure  which  may  be  regarded  as  un- 
failing indications  that  the  rock  possessing  them  has  crystallized  out  of 
a molten  magma. 

An  explanation  for  these  facts  is  not  difficult  to  find.  The  original 
structures  of  clastic  and  igneous  rocks  are  characteristic  and  essentially 
distinct.  Where  these  remain  there  is  no  danger  of  confusion.  In  the 
process  of  metamorphism,  however,  there  is  a constant  tendency  to  ob- 
literate the  original  features  and  to  substitute  for  them  certain  second- 
ary features.  But  these  latter  depend  altogether  upon  the  chemical 
constitution  of  the  mass  and  the  nature  of  the  metamorphosing  forces, 
and  are  independent  of  both  the  mineral  composition  and  the  structure 
of  the  original  rock.  Hence  it  is  that  rocks  fundamentally  distinct  in 

1 Petrographiaclie  Boitnige  ana  dem  ndrdlicUen  ThUringer  Walde.  Jahrbuch  preuaa,  gcol.  Landes- 
anstalt  fur  1883,  pp.  213-237.  Berlin,  1884. 


196  GREENSTONE  SCHIST  AREAS  OF  MICHIGAN.  [bull. 62. 

both  origin  and  structure  grovr  more  and  more  alike  when  subject  to 
metamorphism.  They  may  finally  become  indistinguishable  and  thus 
their  life  histories  may  be  lost,  but  so  long  as  any  trace  of  the  original 
structure  is  recognizable  it  may  be  relied  upon  as  a safe  guide. 

It  is,  therefore,  a matter  of  prime  importance  in  petrography  to  be 
thoroughly  acquainted  with  original  rock  structures,  and  to  understand 
their  significance.  As  a rule,  those  found  in  igneous  rocks  are  more  un- 
mistakable than  those  which  characterize  clastic  deposits.  For  instance, 
universal  observation,  together  with  numerous  synthetical  experiments 
in  the  laboratory,  has  shown  that  the  peculiar  divergent  radial  struct- 
ure, known  as  the  u ophitic v or  u diabase ” structure,  is  always  the 
product  of  crystallization  from  a molten  mass  of  certain  basic  rocks. 
No  single  observation  has  ever  been  made  to  indicate  that  this  structure 
can  originate  in  a sediment  or  by  any  metamorphism  of  a sediment  5 
hence,  we  are  justified,  when  we  encounter  the  u ophitic”  structure  in 
a rock  (no  matter  how  much  it  may  otherwise  resemble  a sedimentary 
deposit)  in  assuming  that  it  is  of  igneous  origin.  Now,  precisely  this 
characteristic  structure  is  what  we  do  meet  most  frequently  in  the 
greenstones  of  both  the  Menominee  and  the  Marquette  area.  Nor  is  it 
alone  in  the  most  massive  and  apparently  least  altered  specimens  that 
it  is  found ; often  the  most  perfectly  schistose  of  these  green  stones  dis- 
close it,  and  that,  too,  where  none  of  the  mineral  components  have 
escaped  complete  alteration. 

Other  structures,  scarcely  less  typical  of  an  igneous  origin  are  also 
encountered  in  other  of  the  Marquette  and  Menominee  rocks.  Some 
of  these  are : porphyritic  structure , with  well  defined  crystals  and  even 
a zonal  growth ; micropegmatite  and  granophyre  structure , in  granite, 
diorite  and  diabase ; poicilitic  structure,  shown  by  the  hornblende  in  the 
diorite  porphyry  at  Lower  Quiunesec  Falls.  The  skeleton  forms  of  the 
acicular  feldspar  crystals,  still  recognizable  in  the  aphanitic  greenstones 
of  the  Upper  Twin  Fail,  as  well  as  in  thos*e  of  the  southern  Marquette 
and  Negaunee  areas,  are  also  strongly  indicative  of  igneous,  and  per- 
haps also  of  glassy  rocks. 

The  evidence  of  eruptive  origin  afforded  by  the  present  mineral  com- 
ponents of  the  Marquette  and  Menominee  rocks  is  not  so  satisfactory 
as  that  based  on  their  structure.  Nor  is  this  different  from  what  we 
should  expect.  Chemical  metamorphism  precedes  structural  metamor- 
phism. Instances  are  frequent  in  both  regions  of  the  disappearance  of 
every  original  mineral,  while  the  structure  remains  intact.  If  we  except 
the  comparatively  recent  and  unaltered  diabases  near  Marquette,  pyrox- 
ene— that  most  characteristic  of  volcanic  minerals — was  hardly  ever  en- 
countered except  in  the  gabbro  at  Sturgeon  Falls.  We  can,  however, 
assert  with  certainty  that  it  was  once  present  in  many  other  rocks, 
where  it  is  now  represented  by  the  pale  green  hornblende  into  which  it 
so  readily  passes.  Other  species  typical  of  igneous  rocks,  such  as  lath- 


GABRRO  AND  DIABASE. 


WILLIAMS.] 


19? 


shaped  labradorite  crystals  and  ilmenite  fringed  with  leucoxene,  on  the 
other  hand,  are  still  met  with  in  abundance. 

With  such  evidence  that  the  greenstones  and  associated  acid  rocks 
of  the  Menominee  and  Marquette  regions  are  igneous  in  their  origin, 
we  may  next  inquire  as  to  how  many  different  types  may  still  with  cer- 
tainty be  recognized  among  them.  In  this  section,  whose  effort  it  is 
to  reconstruct  the  original  form  of  the  greenstones,  no  reference  will 
be  made  to  the  secondary  or  metamorphic  rock-types. 


DIFFERENT  ORIGINAL  ROCK-TYPES. 

BASIC'  BOCKS. 

Olivine  Gabbro. — This  type,  containing  abundant  and  perfectly  crys- 
tallized olivine,  was  found  only  in  the  northern  area  above  Negaunee  ; 
(See  Chap.  V,  p.  180);  and  even  here  under  circumstances  which  left 
doubt  as  to  whether  the  exposure  was  in  situ,  or  a part  of  a huge,  buried 
glacial  bowlder. 

Gabbro. — The  only  undoubted  representatives  of  this  type,  i.  e.,  gran- 
ular aggregates  of  allotriom orphic  diallage  and  plagioclase,  were  found 
at  Sturgeon  Falls  on  the  Menominee  Eiver.  Their  diallage  is  of  an 
unusually  pale  color  and,  like  the  whole  rock,  remarkably  poor  in  iron, 
(cf.  analysis  on  p.  76.)  Their  feldspar  is  almost  wholly  changed  to 
saussurite.  The  rock  exposed  near  the  Eureka  shaft,  two  miles  west 
of  Marquette,  appears  once  to  have  belonged  to  this  same  type  (p.  70); 
while  the  granular  diorites  so  common  at  the  Quinnesec  Falls,  although 
they  now  contain  only  pale  green  hornblende  and  no  diallage,  agree  so 
closely  with  the  Sturgeon  Falls  rock  in  appearance,  structure,  and  chem- 
ical composition,  that  it  is  very  probable  that  they  were  once  gabbros 
also  (pp.  86,  102). 

Diabase. — This  is  by  far  the  most  common  rock-type  and  it  is  found 
in  every  variety  and  stage  of  alteration. 

An  unaltered  olivine  diabase  is  the  youngest  rock  of  the  Marquette 
area.  It  intersects  all  the  other  greenstones  as  well  as  the  granite,  as 
may  be'seeu  at  the  mouth  of  Dead  Eiver,  besides  occurring  in  inter- 
bedded  sheets  in  the  iron  bearing  series  itself.  It  forms  the  great  dike 
which  terminates  at  Lighthouse  Point,  as  well  as  many  other  smaller 
ones  exposed  in  the  Brook  Section,  in  the  northern  area  and  at  other 
localities.  As  the  olivine  is  the  first  of  all  minerals  to  disappear,  this 
type  can,  of  course,  be  recognized  only  in  the  freshest  specimens. 

It  is  not  always  possible  to  say  positively  whether  the  quartz  in  the 
diabase  is  an  original  or  a secondary  constituent.  The  formor,  how- 
ever, is  probably  the  case  in  certain  very  fresh  specimens  and  where, 
as  in  No.  11675  from  the  great  dike,  and  No.  11646  from  Front  street, 
Marquette,  it  is  present  as  a micropegmatitic  intergrowtli  with  the 
feldspar  (p.  141). 

No  non-olivinitie  diabase  was  discovered  in  a perfectly  fresh  state,  but 
this  type  is  assumed  for  many  occurrences  in  which  alteration  is  more  or 


198  greenstone  schist  areas  of  Michigan.  I BULL.  62. 

less  advanced.  Such  an  assumption  mast,  however,  be  doubtful,  since 
any  original  olivine  would  have  been  the  first  mineral  to  disappear. 

Diabase  Porphyry .• — It  is  now  impossible  to  say  whether  the  porphy- 
ritic  greenstones  occurring  at  the  western  end  of  the  ridge  below  the 
Lower  Quiunesec  Falls  once  belonged  to  this  type  or  not.  If  they  did, 
they  contained  considerable  original  brown  hornblende  as  an  accessory 
constituent;  but  it  seems  more  probable  that  these  rocks  were  diorites. 

Glassy  Diabase  and  Melaphyre. — From  the  sides  of  the  unaltered  dia- 
base dikes,  glassy  and  half  glassy  rocks  were  obtained,  which,  of 
course,  represent  only  a local  facies  of  the  main  mass,  due  to  more  rapid 
cooling.  They  contain  incomplete  and  skeleton  forms  of  the  minerals 
which  were  the  first  to  crystallize,  and  in  this  respect  they  closely  re- 
semble some  of  the  aphanitic  greenstones  of  the  southern  Marquette 
and  Negaunee  areas.  Indeed,  one  of  these  half  glassy  rocks  from  the 
edge  of  a much  altered  dike  in  the  Brook  Section,  near  Marquette  (No, 
11680,  see  p.  144),  is  quite  identical  with  a certain  widespread  variety  of 
the  fine  grained  greenstones,  and  gives  perhaps  the  clew  for  the  decipher- 
ing of  their  original  form  (cf.  p.  163). 

. Diorite. — The  readiness  with  which  the  i^roxeue  of  eruptive  rocks 
passes  over  into  a corresponding  amphibole,  makes  the  number  of  dior- 
ites among  the  Menominee  and  Marquette  greenstones  appear  much 
larger  than  it  really  is.  A majority  of  these  are  undoubtedly  of  second- 
ary origin,  having  been  derived  from  pyroxene  rocks.  Nevertheless, 
others  of  them,  in  which  the  secondary  hornblende  can  be  traced  back 
into  a compact  brown  variety  of  the  same  mineral,  must  be  regarded  as 
true  diorites,  unless  we  make  the  assumption  that  pyroxene  has  passed 
by  paramorphism  first  into  basaltic,  and  subsequently  into  fibrous  green 
hornblende.  The  origin  of  other  of  the  dioritic  greenstones  must 
always  remain  uncertain.  Even  at  the  risk  of  including  some  rocks  of 
secondary  origin,  the  principal  dioritic  types  may  be  enumerated  as  fol- 
lows : Gabbro  type — light  colored,  granular  rocks,  like  those  forming  the 
barrier  at  Upper  Quiunesec  Falls ; these  so  closely  resemble  the  Stur- 
geon Falls  gabbro  (even  down  to  the  orthopinacoidal  parting\of  their 
hornblende)  that  there  is  strong  reason  to  believe  that  they  have  been 
derived  from  a similar  rock.  Coarse  grained  diorite  of  the  Horse  Race, 
with  idiomorphic  feldspar  and  a pale  green  hornblende,  which,  though 
itseif  secondary,  has  probably  been  formed  from  a compact  variety  of 
the  same  species.  Granular  diorite , like  No.  11175  from  Four-Foot  Falls 
and  several  dike-rocks  in  the  Negaunee  and  Northern  areas.  Quartz 
diorite,  like  the  Picuic  Island  rock  and  No.  1 1 S3 J , from  the  Northern 
area,  west  of  Marquette.  (See  Plate  IX,  fig.  2.)  Both  of  these  are  per- 
haps more  properly  amphibole  granites,  although  the  relative  propor- 
tions of  their  orthoclase  and  triclinic  feldspar  leaves  this  indoubt.  The 
so-called  u epidiorites  v are  undoubtedly  of  secondary  origin,  and  have 
been  derived  generally  from  augitic  rocks. 


WILLIAMS.] 


ORIGINAL  MINERAL  CONSTITUENTS. 


199 


Biorite  Porphyry . — The  rocks  containing  large  poicilitic  hornblende 
crystals,  collected  from  the  western  end  of  the  ridge  below  the  Little 
Quiunesec  Falls,  which  have  already  been  mentioned  under  the  head  of 
Diabase  Porphyry,  although  they  should  perhaps  receive  the  above 
designation. 

Tuffs. — The  schistose,  banded  greenstones  which  compose  so  large  a 
part  of  the  northern  Marquette  area  are  found  to  be  best  explained  as 
tuff  deposits  of  the  basic  eruptives  which  accompany  them. 

ACID  ROCKS. 

Granite. — Each  of  the  greenstone  areas  is  bounded  on  both  the  north 
and  south  by  a large  mass  of  granite.  This  rock  is  a typical  granitite 
as  can  be  best  seen  from  the  specimens  collected  south  of  the  Horse 
Pace  in  the  Menominee  Yallev  and  north  of  the  Marquette  greenstone 
belt.  Muscovite  granite  occurs  in  some  of  the  bosses  near  Marquette, 
notably  at  the  so  called  u gold  mine 99  near  Pine  street.  Amphibole 
granite  is  possibly  represented  in  the  specimens  from  Picnic  Islands  and 
the  Northern  area  which  have  already  been  mentioned  under  the  head 
of  Quartz  Diorite,  although  they  appear  to  occupy  a position  midway 
between  these  two  types. 

Granite  Porphyry  and  Quartz  Porphyry  are  the  forms  assumed  by  the 
granite  where  it  penetrates  the  greenstones  in  dikes  or  apophyses. 
They  are  abundant  in  both  areas  and  are  united  by  a continuous  series 
of  transitional  forms.  These  rocks  are  among  the  most  interesting  ones 
anywhere  met  with  on  account  of  the  perfection  with  which  they  show 
the  effects  of  dynamic  action.  By  either  stretching  or  compression 
they  are  changed  into  Augen  gneiss  or  schistose  porphyry,  both  of  which 
retain  in  their  microscopic  structure  very  plain  evidence  of  the  manner 
in  which  they  were  produced. 

ORIGINAL  MINERAL  CONSTITUENTS. 

Orthoclase  occurs  in  all  the  acid  rocks — granites,  and  porphyries  $ in 
some  of  the  fragmental  rock,  as,  for  instance,  those  near  Iron  Mount- 
ain and  in  the  stretched  tuffs  on  the  Carp  River  north  of  Teal  Lake, 
and  probably  in  the  Picnic  Island  rock  north  of  Marquette. 

Microcline. — It  is  doubtful  whether  this  form  of  potash  feldspar  is 
ever  original.  In  some  cases  at  least  it  is  certainly  the  result  of  intense 
dynamic  action  on  rocks  already  solid. 

Oligoclase  is,  in  all  probability,  the  species  of  striated  feldspar  occur- 
ring in  the  granites. 

Lahradorice  is  the  prevailing  original  feldspar  in  all  the  greenstones, 
as  it  is  in  the  unaltered  diabases  occuring  near  Marquette. 

Quartz  is  an  abundant  component  of  all  the  acid  types  \ and  it  occurs 
also  in  both  diorites  and  diabases,  although  it  is  here  not  always  pos- 
sible to  distinguish  between  what  is  original  and  what  is  secondary. 

Muscovite  seems  to  exist  in  one  or  two  granites  as  a primary  compo- 
nent, but  in  the  majority  of  cases  it  is  a derivative  of  the  orthoclase. 


200 


GREENSTONE  SCHIST  AREAS  OF  MICHIGAN. 


{bull.  62. 


Biotite  is  abundant  in  the  granites.  It  is  also  present  in  the  diorites, 
especially  in  those  from  the  Horse  Race  Rapid,  although  here  It  may 
be  secondarily  developed  out  of  the  hornblende.  In  the  diabase  it  is 
sometimes  seen  forming  a border  around  the  ilmenite. 

Hornblende. — Compact  brown,  or  basaltic  hornblende  is  common  in 
very  many  of  the  greenstones,  though  mostly  as  remnants  of  crystals 
which  have  become  partly  green  or  fibrous.  It  is  also  present  in  the 
Sturgeon  Falls  gabbro  and  in  the  Marquette  olivine  diabase.  Compact 
green  hornblende  is  also  a very  common  mineral  in  the  greenstones,  but 
it  impossible  to  tell  to  how  great  a degree  this  may  be  of  secondary  origi n. 

.Diallage  of  a very  pale  color  and  very  poor  in  iron  is  abundant  in  the 
gabbro  of  Sturgeon  Falls.  (See  PI.  YHI,  fig.  1.) 

Augite  of  the  ordinary  kind,  having  a reddish  brown  color  in  trans- 
mitted light,  is  an  essential  ingredient  of  all  the  fresher  diabases  ; and 
often  exists  as  a core  in  the  center  of  partially  uralitized  crystals. 

Olivine , in  fresh  and  perfectly  formed  crystals,  was  found  in  the  oli- 
vine gabbro  of  doubtful  origin  which  occurred  in  the  Northern  area 
above  Negaunee.  It  also  once  formed  a component  of  the  younger  dia- 
bases near  Marquette,  although  it  is  now  so  altered  to  serpentine  as  to 
be, only  recognizable  by  its  form. 

Zircon  is  abundant  in  nearly  all  the  acid  rocks,  and  is  present  in  the 
sediments  near  Iron  Mountain  in  the  Menominee  valley.  (No.  11113.) 

Apatite  is  universal  in  all  the  rocks  which  have  not  been  sufficiently 
altered  to  obscure  it. 

Tourmaline  is  common  in  the  more  acid  rocks.  It  may  be  best  seen 
in  the  granite  and  acid  dikes  near  the  Horse  Race  and  Upper  Quinue- 
sec  Falls.  It  is  also  present  in  the  sediments  exposed  near  Iron  Mount- 
ain and  Four-Foot  Falls,  as  well  as  in  the  hornfels  (No.  11064.) 

S phene  occurs  in  both  granite  and  diorite,  especially  in  association 
with  hornblende.  In  some  instances  it  seems  to  have  been  derived 
from  the  alteration  of  ilmenite. 

Orihite  ( Allanite ) is  present  in  certain  granites,  both  near  the  Horse 
Race  and  in  the  Northern  area  above  Negaunee. 

Ilmenite  and  Magnetite. — The  opaque  iron  oxide  minerals  are  present 
in  all  the  rocks  in  their  usual  abundance.  Ilmenite  is  the  most  fre- 
quent, especially  in  the  greenstones,  but  magnetite  is  also  present. 

CONDITIONS  UNDER  WHICH  THE  GREENSTONES  WERE  FORMED. 

There  is  considerable  evidence  to  show  that  the  greenstones,  both  of 
the  Menominee  and  the  Marquette  region,  solidified  at  the  surface, 
under  subaerial  or  subaqueous  conditions. 

In  the  Menominee  Valley  this  evidence  consists  (1)  of  the  fine  text- 
ure of  the  rocks ; and  (2)  of  the  alternation  of  bands  of  different  types, 
which  probably  in  their  original  position  represented  successive  flows. 
Finenessof  grain  is  universal  in  the  Menominee  greenstones,  and  we  may 
be  certain  that  it  was  a primary  feature  in  spite  of  the  extensive  alter- 


WILLIAMS.] 


MACROSTRUCTURAL  METAMORPHISM. 


201 


ation  of  these  rocks.  Tt  is  especially  noticeable  in  the  case  of  the  gab- 
bro,  which  is  almost  always  a coarse  grained  rock  when  it  has  solidified 
at  any  depth.  The  succession  of  massive  beds,  like  the  pale  gabbros 
and  the  dark  diabases  seen  at  Lower  Quinnesec  Falls,  are  difficult 
to  account  for  except  by  supposing  that  they  were  once  horizontal 
sheets  which  flowed  one  over  another  and  which  were  subsequently  ele- 
vated into  their  present  nearly  vertical  position.  Traces  of  tuff  mate- 
rial are  not  as  distinct  here  as  in  the  Marquette  region,  although  indi- 
cations of  their  existence  are  by  no  means  wanting.  We  might  reason- 
ably expect  that  any  original  scoriaceous  or  amygdaloidal  structure 
would  have  disappeared  in  the  course  of  the  profound  chemical  changes 
through  Which  these  greenstones  have  passed. 

In  the  Marquette  area  proof  of  the  superficial  origin  of  the  green- 
stones may  be  found  (1)  in  the  fineness  of  grain,  and  (2)  in  the  frag- 
mental detritus  or  tuff,  such  as  would  accompany  volcanic  action.  The 
so  called  u aphanitic  greenstones,”  which  play  so  important  a role  in  the 
southern  Marquette  and  Xegaunee  districts,  have  traces  of  a structure 
like  that  of  a porphyrite  or  melapbyre  (see  PI.  X,  fig.  2).  At  least 
there  are  incomplete  forms  of  feldspar  crystals  apparently  imbedded  in 
a groundmass  which  might  easily  have  originated  from  the  devitrifica- 
tion and  decomposition  of  a cryptocrystalline  or  even  glassy  base.  The 
finely  banded  greenstone  schists  occupying  the  northern  portion  of  the 
Marquette  belt  present  such  strong  evidence  of  stratification  and  such 
peculiarities  of  microscopic  structure  (see  PI  XVI,  fig.  1)  that  they  are 
best  explained  as  tuff  deposits  belonging  to  the  massive  basic  rocks. 
The  presence  of  fragmental  material  of  this  kind,  of  course,  strongly 
indicates  surface  origin  for  all  these  greenstones.  Still  other  signs 
point  in  the  same  direction.  At  least  one  well  marked  specimen  of 
amygdaloidal  structure  (Xo.  11746)  was  found  near  Baldwin’s  Kilns,  but 
in  the  present  highly  altered  condition  of  these  rocks  it  can  only  occa- 
sion surprise  that  even  this  was  preserved. 

MACROSTRUCTURAL  METAMORPHISM  OF  THE  MENOMINEE  AND  MAR- 
QUETTE MASSIVE  ROCKS. 

This  embraces  all  modifications  in  the  structure  of  the  massive  rocks 
produced  by  dynamic  agencies  and  plainly  visible  to  the  unaided  eye. 
Such  changes  consist  for  the  most  part  in  the  production  of  a banding, 
foliation,  or  schistose  structure,  which  tend  to  make  the  eruptive  rocks 
resemble  stratified  deposits.  They  are  a secondary  feature  and  must 
be  correlated  with  the  slaty  cleavage,  not  with  the  original  bedding  of 
sediments. 

Inthe  process  of  upheaval  and  folding  rocks  may  be  subjected  to  great 
compression,  with  more  or  less  attendant  shearing  or  faulting,  or  the  re- 
verse may  be  true  and  a tension  result.  In  the  first  case  foliation  is 
produced  ; in  the  second,  the  phenomena  of  stretching. 


202 


GREENSTONE  SCHIST  AREAS  OF  MICHIGAN. 


[hull.  62. 


MACRQ8TRUCTURAL  METAMORPHISM  THROUGH  COMPRESSION,  FAULTING,  OR  CRUSHING. 

Simple  compression. — There  seems  to  be  no  doubt  that  a foliation  or 
slaty  cleavage  may  be  produced  by  pressure  in  massive  as  well  as  in 
stratified  rocks.  This  cleavage  is  developed  in  all  cases  at  right 
angles  to  the  direction  of  the  pressure.  It  is  particularly  frequent  in 
such  basic  eruptive  rocks  as,  by  their  chemical  composition,  are  more 
subject  to  alteration.  In  these  the  secondary  development  of  such 
cleavable  minerals  as  chlorite,  hornblende,  sericite,  and  biotite,  which 
are  given  a parallel  arrangement  by  crystallizing  under  pressure, 
sfrongly  conduces  to  the  production  of  a schistose  structure.  The 
pressure  accelerates  the  chemical  action,  and  may  in  this  way  de- 
velop a schistose  out  of  a massive  rock  without  movement  in  the  mass. 

A very  general  feature  in  the  foliated  greenstones  of  both  the  Me- 
nominee and  Marquette  regions  is  their  tendency  to  cleave  parallel  to 
a line  instead  of  parallel  to  a plane;  in  other  words,  they  possess  a 
dip  but  no  decided  strike.  The  rock  then  breaks  with  readiness  into 
loug  rhomboidal  prisms  with  almost  any  angle,  but  is  severed  with 
difficulty  at  right  angles  to  this  axis  of  foliation.  Such  a structure 
would  seem  to  indicate  the  action  of  an  unequal  or  shifting  pressure. 
Examples  of  this  method  of  parting  are  very  common,  especially  at 
Sturgeon,  Lower  Quinnesec,  and  Twin  Falls,  in  the  Menominee  Valley, 
and  in  the  southern  portion  of  the  Marquette  greenstone  area. 

One  of  the  best  proofs  of  the  secondary  origin  through  dynamic 
agency  of  the  greenstone  foliation  is  the  fact,  noticed  by  Major  Brooks, 
that  at  Four-Foot  Falls  this  is  parallel  to  the  slaty  cleavage,  but  not  to 
the  bedding  of  adjoining  sediments. 

Another  method  by  which  a schistose  structure  is  produced  in  the  Me- 
nominee greenstones,  is  the  gradual  flattening  of  the  rhomboidal  prisms 
which  are  formed  by  the  intersection  of  two  sets  of  joint-planes.  This 
is  illustrated  by  Figs.  20,  21,  and  22,  on  page  128.  These  prisms  seem 
to  be  elongated  by  the  action  of  intense  pressure  into  a series  of  inter- 
lacing lenses.  A sort  of  “ Flaser 77  structure  is  thus  produced  which,  in 
its  extreme  development,  becomes  a well  characterized  schistose  struct, 
ure.  Even  in  the  broadest  of  these  prisms  a latent  cleavage  is  often 
noticeable  parallel  to  their  longest  diagonal,  always  following  the 
general  strike  of  the  adjoining  rocks.  This  structure,  which  I have 
designated  as  rhomboidal,  or  diamond  parting,  may  best  be  seen  at  the 
Twin  Falls  or  at  the  upper  end  of  the  great  greenstone  ridge  below 
Lower  Quinnesec  Falls. 

Faulting  or  crushing. — A schistose  structure  is  always  produced  in 
massive  rocks  along  lines  where  a great  tension  has  been  relieved  by 
breaking  and  a consequent  displacement.  Movement  of  this  kind  within 
a solid  mass,  must  be  accompanied  by  more  or  less  intense  crushing, 
and  this  allows  increased  circulation  and  lienee  of  the  rapid  production 
of  secondary  crystallizations.  Admirable  instances  of  this  phenom- 


WILLIAMS.  ] 


FAULTING  OR  CRUSHING. 


203 


euou  abouud  in  both  the  Menominee  and  Marquette  greenstones.  At 
the  Sturgeon  Falls,  along  the  basin  just  below  Lower  Quiunesec  Falls? 
below  the  Horse  Bace,  at  the  Twin  Falls,  at  the  foot  of  Arch  street, 
Marquette,  and  at  many  other  localities  within  this  area,  it  maybe  seen 
with  remarkable  distinctness.  The  exact  effect  of  the  crushing  on  the 
original  mineral  constituents  is  visible  only  under  the  microscope  and 
hence  will  be  considered  in  the  succeeding  chapter ; but  any  one  who 
will  carefully  examine  any  of  the  above  named  localities  can  not  fail  to 
be  convinced  of  the  continuity  and  original  identity  of  the  massive  and 
schistose  rocks. 

Both  the  width  of  these  schistose  blinds  and  the  intensity  of  the 
crushing  which  they  exhibit  vary  widely  in  different  cases.  Their  di. 
rection  almost  always  coincides  with  the  general  strike,  although  at 
Upper  Twin  Falls  such  bands  were  observed  to  have  a different  direc- 
tion. (Seep.  132.) 

This  pulverization  of  the  rock  is  accompanied  by  greatly  increased 
chemical  action  (except  in  the  notable  instance  of  the  feldspar)  and  the 
abundant  production  of  chlorite.  Such  crushed  bands  possess  a more 
or  less  perfect  lenticular  or  u Flaser  ” structure,  which  passes  gradually 
into  a lamination  where  the  action  has  been  more  intense.  This  is  al- 
most entirely  due  to  the  parallel  arrangement  of  the  secondary  chlorite 
scales,  so  that  we  have  a basic  eruptive  rock  developing  into  a typical 
chlorite  schist. 

Excellent  examples  of  a massive,  though  much  altered  greenstone 
fraying  out  into  a chlorite  schist  by  the  action  of  a shearing  force  along 
lines  of  slight  displacement,  were  found  at  lower  Twin  Falls,  and  are 
illustrated  in  Figs.  23  and  24.  (See  pp.  129,  130.) 

The  great  mechanical  force  generated  in  the  course  of  orographic 
movements,  aided  by  chemical  action,  sometimes  develops  schistose 
bands  in  massive  rocks,  which  wind  around  and  encircle  compact  cores. 
These  are  spheroidal  or  lenticular  in  shape,  and  seem  for  some  unknown 
reason  to  have  better  resisted  the  metamorphosing  influences.  A tine 
example  of  this  kind  may  be  seen  on  the  Wisconsin  side  of  the  Menom- 
inee Eiver,  just  at  the  foot  of  Lower  Quinnesec  Falls.  It  is  repre- 
sented by  specimens  ]STos.  11017  to  11020,  described  on  p.  93.  Other 
examples  of  the  same  kind  occur  in  the  railroad  cut  near  Front  street, 
Marquette. 

This  last  described  structure  has  much  in  common  with  the  spheroidal 
or  lenticular  parting  observed  in  the  aphanitic  greenstones  of  the  south- 
ern Marquette  and  Negaunee  areas.  (See  Figs.  26  and  27,  pp.  166, 177.) 
Near  the  mouth  of  Whetstone  Brook $ in  the  neighborhood  of  Bald- 
win’s Kilns,  and  between  Teal  Lake  and  the  Carp. Eiver,  we  see  the  tine- 
grained  greenstones  broken  up  into  circular  or  oval  areas,  which  are 
separated  by  a finer  schistose  matrix.  This  structure  is  common 
through  the  Northwest,  and  has  been  termed  by  the  Canadian  geolo- 
gists “concretionary  trap.”  It  is,  however,  in  no  sense  really  concre- 


204 


GREENSTONE  SCHIST  AREAS  OF  MICHIGAN. 


[BULL.  62. 


tionary,  bat  must  be  ascribed  either  to  contraction  which  frequently 
produces  a perlitic  structure  or  spheroidal  parting  in  volcanic  rocks,  or 
to  a mechanical  brecciation  and  rubbing  together  of  the  disjointed 
fragments,  as  was  found  by  Rothpletz  to  be  the  case  in  similar  green- 
stone schists  of  Saxony.  (See  p.  167.) 

MACROSTRUCTURAL  METAMORPHISM  THROUGH  STRETCHING. 

The  effect  of  stretching  upon  rock  masses  has  only  recently  come  to 
engage  the  attention  of  geologists.  It  is  evident  that  in  the  process  of 
the  upheaval  or  folding  some  parts  of  the  mass  must  be  strained,  while 
other  parts  are  compressed.  As  Heim  first  pointed  out,  such  a tension 
is  relieved  sometimes  with  and  sometimes  without  a visible  rupture. 
Both  of  these  methods  are  well  illustrated  in  the  massive  rocks  of  the 
Menominee  and  Marquette  regions. 

In  the  first  case  we  find  the  formation  of  irregular,  ragged  seams, 
which  Heim  has  designated  as  gaping  rents  (“  klaffende  Risse”),  and 
which  I have  termed  u cross-gashes,”  from  their  being  torn  open  in  a 
direction  perpendicular  to  that  in  which  the  tension  was  exerted.  They 
are,  therefore,  approximately  parallel,  and  may  produce  a rough  sort 
of  schistose  structure.  These  seams  sometimes  remain  open,  but  are 
sometimes  filled  with  secondary  crystallizations,  like  quartz,  calcite,  or 
chlorite,  often  with  epidote.  They  are  best  exhibited  in  the  great 
greenstone  ridge  which  extends  along  the  river’s  left  bank  below  Lower 
Quinnesec  Falls.  Their  appearance,  as  far  as  it  can  be  shown  in  a hand- 
specimen,  is  represented  in  Fig.  10,  p.  81. 

The  manner  in  which  the  round  cores  of  the  spheroidally  parted 
greenstones  in  some  cases  have  been  drawn  out  into  interlacing  lenses, 
has  already  been  noted  (p.  177). 

Stretching  action  may  sometimes  produce  a banding  in  massive  rocks. 
This  is  especially  the  case  with  acid  types,  like  granite  and  quartz  por- 
phyry. Examples  of  this  are  to  be  found  among  the  acid  dikes  near 
the  Horse  Race  and  in  the  vicinity  of  Marquette,  but  the  most  indubi- 
table evidence  of  stretching  in  these  rocks  is  contained  in  their  micro- 
scopic structure,  and  must  therefore  be  reserved  for  description  in  the 
following  section. 

MICROSTRUCTURAL  METAMORPHISM  OF  THE  MENOMINEE  AND  MAR- 
QUETTE MASSIVE  ROCKS. 

Where  profound  mechanical  and  chemical  changes  have  gone  on  si- 
multaneously in  rock  masses,  the  final  product  may  be  wholly  different 
from  the  original  starting  point.  Sedimentary  and  eruptive  rocks  seem 
to  approach  each  other  more  and  more  nearly,  the  longer  they  are  ex- 
posed to  the  same  metamorphosing  influences.  In  many  cases  the  deri- 
vation of  certain  schists  can  never  be  definitely  settled  ; in  other  cases, 
however,  where  the  field  evidence  is  insufficient  to  decide,  the  micro- 


WILLIAMS.] 


EFFECT  OF  DYNAMIC  ACTION. 


205 


scope  may  yield  reliable  data  for  settling  the  origin  of  doubtful  crystal- 
line schists.  Characteristic  minerals  or  structures  may  often  be  de- 
tected under  the  microscope  after  every  original  feature  visible  to  the 
unaided  eye  has  been  obliterated. 

In  stating  the  results  of  dynamic  action  observed  with  a microscope 
in  the  Lake  Superior  rocks,  we  may  speak  first  of  the  effect  upon  individ- 
ual minerals,  and  then  of  new  structures  produced.  As  a rule,  those 
minerals  and  rocks  which  are  hardest  and  most  brittle  are  found  to 
exhibit  these  mechanical  effects  most  perfectly. 

EFFECTS  OF  DYNAMIC  ACTION  ON  INDIVIDUAL  MINERALS. 

Quartz.— We  find  corroborative  evidence  of  the  fact  stated  by  others 
that  quartz  is  frequently  more  sensitive  to  pressure  than  feldspar.  In 
the  quartz  porphyry,  No.  11707,  for  instance  (see  PI.  XY,  fig.  2), 
which  has  undergone  a violent  stretching,  the  feldspar  crystals  appar- 
ently exhibit  no  resultant  phenomena,  if  we  except  the  presence  in  their 
center  of  microcline  as  a possible  product  of  strain  ; the  quartz  crystals, 
on  the  other  hand,  show' an  unusual  amount  of  deformation.  In  some 
cases  they  are  pinched  out  into  pear  or  spindle  shaped  areas  with  an 
undulatory  extinction ; while  in  other  cases  they  are  much  more 
elongated,  but  show  that  this  result  has  not  been  reached  without  a 
crushing  and  displacement  of  their  original  substance  (granulation). 
The  fragments  are  converted  into  a mosaic  of  interlocking  grains  by  the 
readiness  with  which  silica  is  dissolved  and  deposited.  Quartz  that  is 
more  or  less  optically  disturbed  is  almost  universal  in  the  acid  rocks 
examined,  showing  that  hardly  any  of  them  have  been  entirely  free  from 
mechanical  strains.  That  the  quartz  grains  in  the  granite  No.  11104 
are  not  all  original  is  proved  by  the  little  tourmaline  crystal,  which  is 
fractured  and  faulted  at  the  junction  of  two  of  them,  as  depicted  in  Fig. 
13,  p.  112. 

Feldspar. — The  first  effect  of  strain  on  feldspar  is  to  produce  an  un- 
dulatory extinction.  This  cannot,  however,  be  carried  as  far  as  it  is  in 
quartz,  because  the  tension  is  here  able  to  relieve  itself  by  molecular 
movements  and  the  consequent  formation  of  twinning  lamellm.  Sev- 
eral cases  were  encountered  where  the  gridiron  or  microcline  structure 
appears  to  have  been  secondarily  developed  in  a potash  feldspar  by 
this  means,  as  in  the  granites  Nos.  11104  and  11710  and  in  the  schist- 
ose quartz  porphyry  No.  11707.  Such  a production  of  secondary  or 
strain  lamellae  in  the  triclinic  feldspars  is  by  no  means  unusual. 

Where  the  mechanical  action  is  too  intense  to  produce  mere  optical 
disturbance  or  molecular  gliding  without  rupture,  the  force  of  cohe- 
sion is  entirely  overcome  and  the  feldspar  is  fissured  or  crushed.  In 
case  the  force  is  exerted  as  a tension,  the  fragments  thus  formed  are 
separated,  and  the  spaces  between  them  are  filled  with  secondary  crys- 
tallizations, especially  chlorite.  In  other  cases  the  fragments  are  merely 
faulted  against  one  another.  Such  examples  of  stretched  and  faulted 
feldspar  are  very  abundant  in  the  schistose  greenstones  and  acid  rocks 


206  GREENSTONE  SCHIST  AREAS  OF  MICHIGAN.  [bull.  62 

of  tlie  Menominee  and  Marquette  districts.  It  is  generally  possible  to 
recognize  what  fragments  once  belonged  together,  as  may  be  seen  by 
an  inspection  of  PI.  IX,  fig.  2,  PI.  XI,  fig.  2,  PI.  X1Y,  figs.  1 and  2,  and 
Fig.  11  on  p.  105.  Even  in  very  schistose  rocks,  which  are  in  other  re- 
spects chemically  much  altered,  these  broken  feldspars  are,  as  a rule, 
unexpectedly  fresh  ; a fact  which  will  receive  particular  attention  in  the 
succeeding  section. 

If  the  mechanical  force  is  still  greater,  a pulverizing  or  granulation  of 
the  feldspar  ensues.  This  is  always  accompanied  by  chemical  action, 
consisting  of  more  or  less  complete  solution  and  recrystallization.  In 
this  way  the  substance  is  molded  into  new  forms,  which  accord  better 
with  the  existing  strains. 

Such  a partial  grauulation  of  a large  porphyritic  feldspar  crystal,  pro- 
ducing one  of  the  lenticular  u Augen  ” of  the  metamorphic  gneisses  of 
the  Horse  Eace,  is  shown  in  PI.  XY,  fig.  1. 

In  the  process  of  feldspar  granulation  the  calcium  is  frequently  re- 
moved, and  the  secondary  mosaic  is  largely  composed  of  albite,  as  was 
first  shown  by  Lossen. 

Pyroxene. — Diallage  is  very  subject  to  mechanical  deformation.  On 
„ account  of  its  relative  softness  and  flexibility  this  consists  mostly  of  the 
bending  or  twisting  of  the  crystals,  or  in  the  occasional  production  of 
twinning  lamellae.  These  phenomena  may  be  well  seen  in  the  almost 
colorless  diallage  of  the  Sturgeon  Falls  gabbro.  Pyroxeue  exists  in  no 
other  of  the  rocks  examined  except  in  those  which  are  too  young  to 
show  any  effects  whatever  of  dynamic  action. 

Hornblende.— Certainly  in  a large  majority  and  possibly  in  all  the 
rocks  which  I have  studied  from  northern  Michigan,  hornblende  is  a 
secondary  product ; since,  then,  it  is  a result  of  metamorphism,  it  is  not 
strange  that  we  rarely  see  in  it  the  effects  of  that  mechanical  action 
which  caused  the  metamorphism. 

Mica. — On  account  of  its  flexibility  mica,  like  diallage,  would  be  well 
fitted  to  exhibit  mechanical  phenomena ; but  the  fact  that,  like  the 
hornblende,  it  is  mostly  a secondary  mineral  in  those  rocks  to  which 
we  have  here  devoted  our  attention,  prevents  such  deformations  from 
being  common. 

Zircon , Tourmaline,  etc. — These  minute  products  of  the  first  crystalli- 
zation in  the  rock  are  often  found  to  be  broken  or  faulted  by  mechani- 
cal action,  as  is  shown  in  Fig.  13,  p.  112,  and  Fig.  18,  p.  122. 

Ilmenite. — The  iron  minerals,  on  account  of  their  opacity,  of  course 
can  exhibit  no  optical  disturbance,  but  their  grains  are  frequently  torn 
apart  just  like  the  feldspar  crystals.  This  has  been  described  in  num- 
erous instances,  and  it  is  represented  in  PI.  XI,  fig.  2. 

NEW  STRUCTURES  PRODUCED  BY  DYNAMIC  ACTION. 

Whenever  the  crushing  of  rocks  by  dynamic  agencies  is  accompanied, 
as  it  almost  always  is,  by  chemical  action  and  the  production  of  new* 
minerals,  these  must  arrange  themselves  in  accordance  with  the  exist* 


WILLIAMS.] 


NEW  STRUCTURES  BY  DYNAMIC  ACTION. 


207 


ing  strains.  These  secondary  minerals  are  such  as  themselves  possess 
a very  perfect  cleavage;  their  production,  therefore,  under  circumstances 
of  uniform  and  continued  strain,  will  naturally  impart  a foliation  to 
the  originally  massive  rock.  Nor  is  this  all.  The  relief  of  the  strain 
and  the  consequent  crushing  of  the  rock  will  take  place  along  certain 
planes  much  more  completely  than  along  others;  hence  in  these  planes 
the  secondary  minerals  will  be  more  abundant,  and  a banding  of  a once 
homogeneous  rock  may  result. 

The  final  structures  produced  in  this  manner  depend  not  altogether 
upon  the  force  exerted,  but  also  upon  the  primary  structure  of  the  rock. 

The  rubbing  together  of  individual  crystal  grains,  the  adhesion  be- 
tween which  is  weaker  than  their  own  internal  cohesion,  may  produce 
a pulverizing  only  around  the  edge,  when  the  force  is  not  too  intense. 
This  phenomenon,  to  which  Professor  Kjerulf  has  applied  the  term 
“peripheral  granulation”  (randliche  Kataklase),1  may  bring  about  a 
sort  of  pseudo-porphyritic  structure,  in  which,  however  the  porphvritic 
crystals  are  only  the  larger  remnants  of  the  former  grains  without  a 
crystal  form  of  their  own  ; or,  if  the  crushing  has  been  less,  the  grains 
may  appear  to  be  held  together  by  a fine  granular  cement,  like  the 
stoues  of  a wall  by  their  mortar.  Hence  Professor  Tornebohm  has 
spoken  of  this  as  the  “mortar  structure”  (Mortel  Structur).2  Many 
admirable  examples  of  these  structures  are  to  be  seen  in  the  Menominee 
and  Marquette  rocks,  especially  in  those  of  an  acid  character.  There 
may  be  particularly  mentioned  the  granite  from  the  great  area  south 
of  the  Menominee,  No.  11104;  Nos.  11189  and  11190  from  acid  dikes  at 
the  Horse  Pace;  Nos.  11678  and  11710  from  the  Brook  Section,  near 
Marquette.  In  the  first  instance,  a distinct  micropegmatitic  structure 
is  a noticeable  feature  of  the  granular  cement. 

If  the  original  structure  of  the  rock  was  porphyritic  instead  of 
granitic,  we  find  corresponding  differences  in  the  result.  The  ground- 
mass  is  made  schistose  by  the  development  out  of  its  feldspar  of  sericite 
or  chlorite.  The  porphyritic  crystals  are  more  or  less  granulated,  but 
the  secondary  mosaic  thus  formed  is  often  coarser  in  grain  than  the 
groundmass.  This  is  arranged  around  the  remnant  of  the  original 
crystal  in  a lenticular  area  known  as  the  “eye,”  or  “Auge,”iu  rocks 
called  by  the  Germans,  on  account  of  this  structure,  Augengneiss.  (See 
PI.  XV,  fig.  1.)  Unusually  beautiful  examples  of  this  kind  are  to  be 
found  among  the  acid  dikes  along  the  shores  of  the  Horse  Race — 
especially  specimens  numbered  11184  and  11196.  In  some  of  the 
schists  which  have  been  derived  from  the  Sturgeon  Falls  gabbros  a sim- 
ilar structure  is  present. 

Where  secondary  micaceous  minerals  have  been  developed  in  sinuous 
bands  which  interlace  and  twine  about  abundant  oval  cores,  a lenticu- 

1 Grmidfjeldsprofilet  ved  Mjoaens  sj  dende.  Nyt  Mag.  for  Naturvidcnskabemo,  vol.  29,  p.  215, 1885 
(Nenes  Jalirbuch  fiir  Mineral.,  1886,  vol.  2,  Referate,  p.  244.) 

’Nigra  ord  om  granit  och  gneis.  Geol.  Foren.  Stockholm  Forhandl,  vol.  5,  pp.  233-248.  (Neues, 
Jahrbuch  fiir  Mineral.,  1881,  vol.  2,  Referate,  p.  50.) 


208 


GREENSTONE  SCHIST  AREAS  OP  MICHIGAN. 


[BULL.  62. 


lar  structure  is  produced,  in  which  there  is  no  contrast  between  ground- 
mass  and  porphyritic  crystals.  This  is  called  by  the  Germans  “ Flaser7’ 
structure,  a term  which  may  advantageously  be  transferred  to  the  Eng- 
lish. It  is  often  the  case  that  a structure  of  this  kind  is  so  fine  as  to  be 
visible  only  under  the  microscope,  when  the  designation  “ microflaser 
structure”  is  applicable.  Examples  of  this  lenticular  interlaciug  are 
abundant  in  the  schistose  greenstones  of  northern  Michigan.  It  is  es- 
pecially typical  in  the  Sturgeon  Falls  schists,  and  in  those  at  Lower 
Quiunesec  Falls ; it  may  also  be  well  seen  in  the  granite  at  the  mouth 
of  the  Dead  Fiver,  north  of  Marquette. 

In  rocks  that  have  been  subjected  to  a great  tension,  a peculiar  micro- 
scopical structure  has  been  developed,  caused  by  the  rupture  of  the 
original  crystals  and  a pulling  apart  of  their  fragments.  Between  these 
chlorite  is  formed,  the  scales  of  which  are  parallel  to  one  another  and 
to  the  direction  of  the  stretching.  This  chlorite  appears  to  have  re- 
sulted from  the  recrystallization  of  the  substance  of  the  original  bisili- 
cates, since  no  trace  of  these  now  remains,  although  the  broken  feldspar 
is  always  remarkably  fresh.  There  must  be  something  in  the  dynamic 
action  of  an  intense  tension  particularly  conducive  to  the  formation  of 
tips  chlorite,  for  exactly  this  modification  of  this  mineral  was  not  en- 
countered in  rocks  produced  in  any  other  way.  Its  presence,  of  course, 
brings  out  a decided  schistose  structure.  Excellent  examples  of  this 
phase  of  structural  metamorphism  abound  in  the  Menominee  and  Mar- 
quette greenstones,  although  I do  not  know  that  anything  exactly  like 
it  (particularly  when  taken  in  connection  with  the  remarkable  freedom 
of  the  broken  feldspar  from  all  signs  of  chemical  change)  has  ever  been 
described  before.  It  is  illustrated  in  PI.  XI,  fig.  2.  The  widely  dif- 
ferent results  produced  in  the  same  greenstone  by  chemical  action  alone 
on  the  one  hand,  and  by  this  agency  combined  with  stretching  on  the 
other,  are  shown  in  PI.  IX,  figs.  1 and  2.  The  same  thing  is  admi- 
rably seen  in  two  specimens  (Nos.  11651  and  11652)  from  the  Cleveland 
ore  dock  in  Marquette.  (See  p.  168.)^ 

If  we  could  desire  any  more  certain  proof  that  these  “stretching 
structures”  are  of  secondary  origin,  developed  in  an  already  solid  rock, 
we  should  find  it  in  No.  11803  (PI.  XIY,  fig.  2).  Here  the  porphyritic 
feldspar  crystals  lie  in  the  groundmass  at  every  conceivable  angle,  show  - 
ing that  at  the  time  they  were  formed  there  was  no  force  to  affect  their 
orientation.  Their  breaking  and  tearing  asunder,  however,  in  every 
case,  has  taken  place  in  the  direction  of  the  foliation  or  stretching, 
without  the  least  reference  to  the  position  of  the  feldspar  crystal  itself. 

MINERALOGICAL  (CHEMICAL)  METAMORPHISM  OF  THE  MENOMINEE 
AND  MARQUETTE  ROCKS. 

Chemical  alteration  may  go  on  to  almost  any  extent  in  massive  rocks, 
unattended  by  any  mechanical  deformation ; and  yet  certain  chemical 
changes  in  rock-forming  minerals  seem  to  be  dependent  upon  the  phys* 


WILLIAMS.] 


PRODUCTS  OF  METAMORPHISM. 


209 


ical  conditions  produced  by  great  orographic  strains.  It  is  easy  to 
understand  how  the  crushing  of  a rock  should,  as  a rule,  accelerate 
chemical  activity  by  increasing  the  circulation  and  possibly  by  raising 
the  temperature  by  friction  ; but  more  than  this,  we  find  that  of  several 
different  alterations  to  which  a given  mineral  is  subject,  certain  ones 
are  never  found  except  in  those  regions  where  dynamic  action  has  been 
intense. 

It  is  true  that  the  same  secondary  mineral  may  be  produced  In  differ, 
ent  ways.  It  may  result  from  the  same  original  mineral  under  different 
conditions,  or  from  different  minerals  under  the  same  conditions,  or  from 
different  minerals  under  different  conditions.  It  may  also  sometimes 
be  derived  from  a single  substance,  and  sometimes  from  a reaction  be- 
tween two  or  more  substances.  On  account  of  the  small  number  of 
elements  which  enter  into  the  composition  of  rock-forming  minerals, 
their  physical  differences  are  due  mostly  to  the  different  proportions  in 
which  these  elements  are  combined.  Very  slight  variation  in  condi- 
tions may  modify  these  proportions  and  so  produce  one  mineral  or 
another.  Even  in  exactly  the  same  chemical  compound,  what  may  be 
a stable  state  under  one  set  of  conditions,  may  be  an  unstable  state 
under  another  set.  So  delicate  is  this  adjustment  that  the  secondary 
minerals  produced  in  a given  case  depend  not  merely  upon  the  chem- 
ical composition  of  the  original  rock  or  of  its  constituents,  but  even  to 
a greater  degree  upon  the  physical  conditions  obtaining  at  the  time  of 
their  formation.  Thus  with  every  change  of  these,  one  generation  of 
secondary  minerals  may  give  place  to  another. 

Such  a succession  of  alterations,  each  dependent  upon  its  owmset  of 
conditions,  teuds  to  obscure  the  life  history  of  a rock  mass ; and  yct^h^ 
spite  of  its  complexity,  this  study  is  full  of  promise.  It  is  generally 
possible  to  separate  the  products  of  metamorphism  proper  from  those 
of  weathering,  as  described  in  Chapter  I (see  p.  36).  All  the  massive 
rocks  of  tbe  Menominee  and  Marquette  regions  offer  admirable  op- 
portunity for  the  study  of  the  first  of  these  alterations,  while  the  more 
basic  types  often  present  the  subsequent  effects  of  weathering. 

In  reviewing  and  summing  up  the  results  of  chemical  alteration 
already  described  at  length,  it  will  be  advantageous  first  to  enumerate 
the  minerals  of  secondary  origin,  stating  briefly  the  circumstances  un- 
der which  each  was  probably  formed,  and  second  to  trace  out  the  differ- 
ent phases  of  alteration  to  which  each  of  the  more  important  original 
constituents  has  been  subjected. 

SECONDARY  MINERALS  AND  THEIR  ORIGIN. 

PRODUCTS  OF  METAMORPIIISM. 

Feldspar. — This  mineral  is  not  common  as  a secondary  product  ex- 
cept in  the  form  of  albite,  which  as  Lossen  has  shown  (see  Chap.  I.  p.  60) 
is  a very  characteristic  result  of  dynamic  metamorphism.  In  the 
Sturgeon  Falls  gabbro  albite  is  a common  secondary  mineral,  both  as 

Bull.  62 14 


210 


GREENSTONE  SCHIST  AREAS  OF  MICHIGAN. 


[ HULL.  62. 


the  base  of  saussutite  and  in  the  form  of  clear,  transparent  veins.  Here 
the  twinning  structure  is  not  frequent,  but  it  may  be  seen  in  some  of  the 
veins,  as  is  shown  in  Fig.  4,  p.  69.  Albite  in  the  form  of  a fine  gran- 
ular mosaic,  with  or  without  quartz  also  occurs  in  many  of  the  altered 
diabases.  Its  substance  is  so  clear  and  glassy  as  to  leave  no  doubt 
about  its  being  a secondary  product. 

Microcline  as  a secondary  mineral  is  to  be  referred  rather  to  the  effect 
of  pressure  twinning  than  to  chemical  alteration. 

Saussurite  (Chapter  I,  p.  58)  is  not  a simple  mineral,  but  a mixture 
derived  from  the  alteration  of  the  lime-soda  feldspars.  It  is  abundant 
in  the  more  basic  rocks  of  the  Menominee  aud  Marquette  regions — in 
the  gabbros  of  Sturgeon  Falls  and  in  many  diabases  and  diorites.  The 
base  is  a clear,  soda  feldspar  (albite)  which  contains  zoisite  needles,  or 
more  rarely  epidote  aud  colorless  garnet.  (No.  11189,  p.  108.) 

Zoisite  occurs  only  as  one  of  the  constituents  of  saussurite  above 
described.  It  is  in  the  form  of  minute  needles,  without  terminations, 
as  shown  in  Figs.  5 and  6 (pp.  69,  70).  These  differ  much  in  size,  and 
between  crossed  nicols  display  dull  bluish  interference  colors.  When 
the  zoisite  needles  are  very  small  the  saussurite  is  a gray  opaque  mass, 
which  only  the  highest  power  of  the  microscope  is  able  to  resolve. 

Garnet  was  observed  only  once,  in  minute  colorless  crystals,  forming, 
along  with  epidote,  one  of  the  constituents  of  the  saussurite  in  speci. 
men  No.  11189.  (see  p.  108). 

Quartz  is  a widespread  secondary  mineral.  It  often  originates  from 
the  breaking  up  of  the  more  acid  feldspars,  like  orthoclase.  It  may  also 
originate  from  the  lime-soda  feldspars.  Primary  and  secondary  quartz 
sometimes  present  an  identical  appearance.  In  some  of  the  Lake  Su- 
perior diabases  quartz  seems  to  be  an  original  component,  and  in  others 
of  the  more  altered  ones  it  is  certainly  of  secondary  origin.  In  a few 
intermediate  cases  its  origin  must  always  remain  doubtful.  Owing  to 
the  ease  with  which  silica  is  transported  in  solution,  that  which  is  set 
free  by  the  decomposition  of  the  silicates  is  often  entirely  removed  from 
the  rock  or  is  deposited  in  seams.  In  at  least  one  instance  a brown 
isotropic  substance  resembling  opal  was  observed  (the  gabbro  from 
Eureka  Shaft  near  Marquette  p.  170). 

Hornblende. — Although  there  is  reason  for  considering  the  hornblende 
in  some  of  the  Menominee  and  Marquette  greenstones  as  a primary 
constituent,  still  there  can  be  no  doubt  that^this  mineral  is  also  the  most 
important  secondary  component  of  these  rocks.  In  a fibrous  form  as 
uralite,  amianth,  etc.,  hornblende  is  almost  the  sole  representative  of 
the  former  pyroxene  in  the  more  altered  and  schistose  diabases,  and  the 
same  mineral  seems  also  to  be  the  final  metamorphic  product  of  the 
compact  hornblende  in  the  diorites.  Indeed,  the  schistose  structure 
of  these  rocks  is  largely  due  to  the  production  of  fibrous  hornblende  and 
lamellar  minerals  of  the  mica  type,  and  to  their  arrangement  parallel 
to  a single  plane.  The  components  of  the  secondary  fibrous  hornblende 


WILLIAMS.] 


SECONDARY  MINERALS. 


211 


are  mainly  derived  from  some  bisilicate,  like  pyroxene  or  compact 
hornblende,  but  its  position  is  by  no  means  confined  to  the  area  formerly 
occupied  by  these  substances.  On  the  contrary,  the  material  shows  a 
tendency  to  wander,  and  to  develop  amphibole  needles  along  the  cleav- 
age cracks  of  the  feldspar,  as  seen  in  Plate  XII,  fig.  2.  This  may  even 
become  filled  with  the  hornblende,  as  in  the  epidiorite,  Xo.  11663,  from 
Pine  street,  Marquette,  and  the  whole  rock  be  finally  reduced  to  a fine, 
felt-like  mass,  as  shown  in  Plate  IX,  fig.  1. 

Compact  hornblende  also,  both  brown  and  green,  appears  to  have  re- 
sulted extensively  in  the  greenstones  from  the  direct  alteration  or 
molecular  rearrangement  of  pyroxene.  Such  a change  has  often  been 
recorded,  as  stated  in  Chap.  I.  Indeed,  the  probability  that  much  of 
the  pyroxene  of  the  original  rocks  has  passed  into  fibrous  green  horn- 
blende through  an  intermediate  stage  of  compact  hornblende  has  already 
been  alluded  to  (p.  72).  The  brown  or  basaltic  variety  is  to  be  found 
associated  with  the  diallage  of  the  Sturgeon  Palls  gabbro,  as  shown  in 
PI.  VIII,  figs.  1 and  2;  also  in  the  porphyritic  rock  from  the  western 
end  of  the  u gabbro  ridge,”  near  Little  Quinnesec  Falls,  on  the  Meno- 
minee. The  compact  green  hornblende  of  Xos.  11176  and  11178,  from 
the  Four-Foot  Fall,  and  of  many  of  the  Horse  Race  diorites,  has  pre- 
cisely the  form  of  diabasic  augite ; and  in  spite  of  its  compact  structure 
shows  in  its  pale  color  and  darker  green  border  clear  evidence  of  its 
secondary  origin.1  The  pale  compact  hornblende  of  the  barrier  rock 
at  Upper  Quinnesec  Falls  (Xo.  11054)  looks  exactly  like  diallage,2  and 
under  the  microscope  its  most  exceptional  orthopinacoidal  parting 
bears  testimony  to  its  derivation  from  this  mineral.  (See  p.  103.) 

The  manner  in  which  the  compact  hornblende  ravels  out  and  becomes 
fibrous  is  often  clearly  seen  in  the  Lake  Superior  greenstones,  and  is 
shown  in  PI.  XII,  fig.  1,  and  in  Fig.  19  on  p.  126. 

Epidote  is  a common  metamorphic  mineral,  and  appears  almost  al- 
ways in  small  but  well  formed  yellowish  crystals.  It  sometimes  forms 
one  of  the  constituents  of  saussurite,  but  far  less  frequently  than  zoisite, 
as  more  iron  is  necessary  for  its  genesis.  In  one  case,  Xo.  11091,  the 
feldspar  of  a coarsely  granular. rock  from  the  Horse  Race,  seems  wholly 
changed  to  large  individuals  of  epidote,  while  the  pyroxene  has  given 
place  to  corresponding  areas  of  a rather  compact  greenish  hornblende  (p. 
108).  In  Xo.  11712,  from  the  Brook  Section,  near  Marquette,  the  change 
of  the  feldspar  to  epidote  is  less  complete.  Epidote  more  commonly 
results  from  the  alteration  (perhaps  weathering)  of  some  ferrous  bisili- 
cate. Here  it  is  generally  in  association  with  bright  green  chlorite  in 
the  form  of  the  characteristic  aggregate  described  in  Chap.  I (p.  56). 
This  is  very  common  in  many  of  the  more  altered  greenstones  of  the 
regions  studied.  (See  PI.  XI,  fig  1.) 

1 See  PI.  XII,  fig.  2;  and  cf.  Loasou  : Erliiut.  zur.  geol.  Spe.cialkarto  von  Preuaaen,  Platt  Ilarz- 
gerode,  1882,  p.  81;  and  William  a’  Bull.  U.  S.  Geol.  Survey,  No.  28,  PI.  I,  fig.  2;  PI.  H,  fig.  1,1886. 

2 cf.  H.  Credner:  Neues  Jahrbuch  fur  Mineral.,  1870,  p.  972. 


212  GREENSTONE  SCHIST  AREAS  OF  MICHIGAN.  [bull.  62. 

Biotite  originates  under  certain  -circumstances  from  hornblende.  This 
is  an  alteration  well  known  to  mineralogists,1  and  may  be  admirably 
seen  in  several  of  the  Horse  Race  diorites  and  in  the  curious  amphi- 
bole  granite,  No.  11831,  figured  in  PI.  XYJ,  fig.  2. 

Muscovite , Sericite . — The  potash  micas  hold  a similar  place  in  relation 
to  orthoclase,  as  a product  of  dynamic  metamorphism,  that  saussurite 
does  to  the  lime^soda  feldspars.  In  some  specimens,  as  for  instance  in 
the  granite  No.  11089  from  the  Horse  Race  and  in  No.  11660  from  the 
so-called  gold  mine  near  Pine  street,  Marquette,  broad  plates  of  typical 
muscovite  are  developed  in  the  feldspar ; generally,  however,  the  alter- 
ation is  due  to  the  minute  scales  or  curved  foliie  called  sericite.  These 
two  minerals  are  quite  identical  in  composition  and  generally  in  origin, 
as  has  been  explained  in  Chap.  I.  The  development  of  sericite  may  be 
best  studied  in  the  schistose  porphyries,  which  owe  their  cleavage  to 
stretching.  These  are  abundant  in  both  the  regions  investigated, 
especially  at  Upper  Quinnesec  Palls  (see  Chap.  Ill,  and  PI.  XIY,  fig. 
3)  and  near  the  city  of  Marquette  (Chap.  IY).  While  the  production 
of  sericite  in  the  acid  rocks  is  for  the  most  part  the  result  of  intense 
dynamic  action,  it  would  seem  as  though  it  were  especially  liable  to  re^ 
suit,  like  certain  varieties  of  chlorite  (see  below),  when  this  force  acted 
as  a tension  rather  than  as  a compression. 

Titanium  minerals. — The  metamorphosed  eruptive  rocks  of  the  re- 
gions studied  offer  unusual  opportunities  for  tracing  the  varied  trans- 
formations of  the  titanium  compounds.  It  is  doubtful  whether  this 
element  existed  in  the  original  rocks  in  any  other  form  than  titanic  iron 
(ilmenite)  or  as  a component  of  certain  biotites.  In  the  metamorphic 
rocks,  however,  titanium  minerals  are  numerous  and  their  origin  can 
be  traced  to  different  sources.  The  probable  derivation  of  rutile  and 
magnetite  from  ilmenite  may  be  seen  in  No.  11070,  from  Upper  Quin- 
nesec Palls  (PI  XIII,  fig.  2),  and  also  in  No.  11825,  from  northwest  of 
Marquette  (p.  181).  The  little  “ Thonscliiefernadeln,”  shown  in  Fig.  12 
(p.  106),  seem  also  to  have  been  derived  from  ilmenites.  A sagenitic 
network  of  rutile  produced  by  the  alteration  of  biotite  and  the  conse- 
quent freeing  of  titanic  oxide  is  seen  in  No.  1111 3, from  Iron  Mountain; 
in  No.  11672  from  Marquette;  and  in  No.  11738,  from  near  Baldwin’s 
Kilns,  Negaunee. 

Anatase,  along  with  leucoxene,  has  resulted  from  the  alteration  of 
ilmenite  in  No.  11130,  from  Twin  Falls  (Fig.  26$  p.  166)  and  in  No. 
11802,  north  of  Negaunee,  near  the  Carp  River.  Anatase  seems  also 
to  have  resulted  from  the  decompositon  of  titaniferous  biotite  in  Nos. 
11050  and  11052,  from  near  Upper  Quinnesec  Falls. 

Sphene  in  the  form  of  leucoxene  is  a universal  result  of  the  alteration 
of  ilmenite  in  the  metamorphosed  diabases.  In  rare  cases,  like  No. 
11014,  from  Lower  Quinnesec  Falls,  it  is  intimately  associated  with 

*See  J.  Roth:  Allgomeine  undcheimsche  Geologie,  vol.  1,  p.333,  1879,  and  Inostrauzeff : Metamor- 
phosirte  Gesteine  im  Gouvernment  Olonez,  1879,  p.  192. 


WILLIAMS  J 


PRODUCTS  OF  WEATHERING. 


213 


rutile,  which  may  have  been  produced  simultaneously  with  the  altera- 
tion of  the  leucoxene,  or  have  resulted  from  it.  In  other  exceptional 
cases  the  product  of  the  ilmenite  appears  with  all  the  crystal  form  and 
physical  properties  of  rock-forming  sphene.  Such  an  occurrence  in  No. 
11189  from  the  Horse  Race  is  shown  in  PI.  XIII,  fig.  1 ; and  another 
in  No.  11831,  from  northwest  of  Marquette,  in  PI.  XVI,  fig.  2. 

The  secondary  minerals  thus  far  enumerated  are  products  of  meta- 
morphism proper,  as  distinguished  from  weathering  j that  is,  they  are 
highly  crystalline,  and  have  been  produced  under  circumstances  very 
different  from  those  ordinarily  prevailing  at  the  earth’s  surface.  Here 
the  tendency  is  for  the  more  crystalline  and  less  soluble  compounds  to 
become  more  soluble  through  union  with  water  and  carbon  dioxide. 
Hydration  and  carbonatization  are  therefore  characteristic  results  of 
surface  action  upon  rocks.  They  bring  about  their  disintegration  and 
decay,  as  purely  metamorphic  processes  do  not.  Both  metamorphism 
and  weathering  are  very  apparent  in  the  eruptive  masses  of  the  Me- 
nominee and  Marquette  regions.  The  rocks  of  Keweenaw  Point,  on 
the  other  hand,  show  only  the  effects  of  weathering.  In  spite  of  their 
great  antiquity  they  have  not  undergone  metamorphism  in  the  strict 
sense.  Much  younger  rocks  in  disturbed  areas  are  often  found  to  be 
intensely  metamorphosed,  which  clearly  shows  that  something  besides 
mere  lapse  of  time  is  necessary  to  accomplish  this  change.1 

PRODUCTS  OF  WEATHERING. 

The  secondary  minerals  in  the  Menominee  and  Marquette  massive 
rocks  which  owe  their  existence  to  atmospheric  action  or  weathering 
belong  mainly  to  the  following  species:  Chlorite,  talc,  serpentine,  car- 
bonates (calcite,  dolomite,  etc.),  iron-hydroxide,  and  pyrite. 

(Jlilorite  is  generally  a product  of  weathering,  but  its  origin  is  some- 
times closely  associated  with  dynamic  agencies.  For  instance,  it  is  a 
constant  feature  in  the  basic  rocks  which  have  been  stretched  (like  se- 
ricite  in  the  more  acid  ones),  filling  with  its  parallel  folia  the  interstices 
between  the  broken  and  separated  fragments,  and  thus  imparting  a 
degree  of  schistosity  to  the  entire  mass,  (see  PI.  XT,  fig.  2.)  The 
ordinary  process  of  chloritization  has  been  described  in  Chapter  I,  and 
frequently  alluded  to  in  the  petrographical  descriptions,  since  it  is  ex- 
tremely common  in  the  basic  eruptives.  If  the  original  mineral  was  very 
poor  in  iron  an  almost  colorless  chlorite  was  the  result,  as  in  the  Stur- 
geon Falls  gabbro  (PI.  VIII,  fig.  2).  In  the  highly  ferruginous  dia- 
bases, on  the  other  hand,  the  chlorite  has  a deep  green  color  and  is 
often  pleochroic.  This  is  the  li  viridite”  of  the  older  authors,  which  is 

1 Tho  efficiency  of  orographic  movements  to  bring  about  this  result  lias  already  been  sufficiently 
emphasized.  The  observations  of  Losson  that  similar  changes  may  be  produced  by  the  contact  action 
of  large  masses  of  intrusive  granite  have  been  briefly  referred  to  in  Chapter  I.  To  what  extent  the 
enormous  granite  areas  lying  on  both  sides  of  the  Marquette  and  Menominee  greenstone  bolts  may 
havo  been  instrumental  in  effecting  their  miueralogical  metamorphism  must  for  tho  present  bo  left 
undecided,  inasmuch  as  no  evidence  directly  bearing  upon  this  question  has  as  yet  been  collected. 


214 


GREENSTONE  SCHIST  AREAS  OF  MICHIGAN. 


[BULL.  62. 


frequently  associated  with  sharply  defined  epidote  (secondary  augite  of 
Wichmann),  as  figured  in  PL  XI,  fig.  1.  Chlorite  seems  to  be  the 
common  effect  of  weathering  upon  pyroxene,  hornblende,  and  biotite. 

The  peculiar  variety  of  chlorite  known  as  “ helminth” in  vermiform 
aggregates  occurs  imbedded  in  secondary  quartz  in  some  of  the  Stur- 
geon Falls  gabbros,  and  is  represented  in  Fig.  8 on  p.  71. 

Talc  results  in  some  cases  from  the  alteration  of  hornblende,  as  ob- 
served by  Tschermak,1  Inostranzeff,2  Becke,3  and  the  writer.4  This  is 
not  a common  phenomenon  in  the  Michigan  greenstones,  but  some  ad- 
mirable examples  were  observed  in  the  coarse  grained  diorites  of  the 
Horse  Bace  above  Upper  Quinnesec  Falls. 

Serpentine. — The  scarcity  of  olivine  in  the  rocks  examined  makes  the 
ordinary  derivation  of  serpentine  uncommon.  This,  however,  does  oc- 
cur in  some  of  the  least  altered  diabases  of  Marquette.  Indeed,  ser- 
pen tinization  is  almost  the  only  effect  of  weathering  noticeable  in  some 
specimens  from  the  great  dike  of  Lighthouse  Point  (olivine  diabase), 
certain  weakly  polarizing  fibers  resulting  from  the  change  of  hornblende 
appear  to  be  serpentine,  which,  according  to  Eosenbusch,5  frequently 
gives  rise  to  this  mineral.  An  instance  of  this  may  be  seen  in  Nos. 
11078  and  11191  from  the  Horse  Race  (p.  109). 

Carbonates. — These  most  frequent  products  of  weathering  abound  in 
the  most  altered  greenstones,  but  they  are  nevertheless  not  unfrequently 
absent  on  account  of  the  readiness  with  which  these  compounds  are 
removed  in  solution.  Calcite  and  dolomite  are  not  microscopically  dis- 
tinguishable without  a chemical  reaction,  but  this  is  hardly  necessary 
for  most  cases. 

Iron-hydroxide  and  Pyrite  are  both  iron  compounds  universally  pro- 
duced in  basic  rocks  under  ordinary  atmospheric  influences.  The  Mich- 
igan greenstones  present  no  exception  in  the  amount  of  these  minerals 
which  they  contain. 

PROGRESS  OP  ALTERATION  IN  THE  ORIGINAL  MINERALS. 

Feldspar  gives  alteration  products  depending  very  largely  upon  its 
original  composition,  whether  alkaline  or  calciferous.  By  far  the  most 
common  change  in  the  more  basic  rocks  is  to  saussurite.  This  varies  in 
different  cases  from  a comparatively  coarse  grained  zoisite  aggregate  to 
a dull  gray,  almost  opaque  mass  which,  even  in  the  thinnest  sections, 
is  beyond  the  highest  power  of  the  microscope  completely  to  resolve. 
The  saussuritization  may  be  often  seen  to  have  proceeded  from  the 
periphery  of  the  feldspar  crystal  inward.  In  such  cases  a compara- 
tively unaltered  center  remains,  as  in  No.  11168  from  Sturgeon  Falls 
(PI.  VIII,  fig.  2).  Quite  as  frequent  is  the  occurrence  of  a clear  per- 

1Tschermak’s  mineral,  u.  petrog.  Mittheil.,  vol.  4,  p.  65,  1876. 

2 Metamorpliosirte  Gesteine  im  Gouvemment  Olonez,  Leipzig,  1879,  p.’  167. 

3Tschennak’s  mineral,  u.  petrog.  Mittheil.,  vol.  4,  1882,  pp.  339  and  349. 

4Bull.  IT.  S.  Geol.  Survey,  No.  28,  p.  58,  1886. 

6Mikroa.  Physiog.,  2d  ed.,  vol.  2,  p.  108. 


Williams.  ] 


ALTERATION  PRODUCTS  OF  FELDSPAR. 


2 15 


ipliery  around,  feldspar  crystals  which  have  been  completely  saussuri- 
tized.  (See  No.  11167  from  Sturgeon  Falls  (PI.  VIII,  fig.  1);  No. 
11054  from  Upper  Quinnesec  Falls,  and  No.  11182  from  the  Horse  Eace.) 
The  clear  feldspar  substance  in  such  cases  appears  like  a new  crystalli- 
zation rather  than  an  unaltered  survival  of  the  original  individual  (cf. 
Fig.  4,  p.  69). 

The  inverse  ratio  existing  between  the  mechanical  and  the  chemical 
action  visible  in  the  altered  feldspars  of  the  basic  rocks  has  been  often 
alluded  to  on  pp.  88,  169.  This  seems  to  be  the  reverse  of  what  might 
be  expected,  as  well  as  of  what  is  actually  observed  in  the  case  of  all 
the  other  constituents.  It  is,  however,  frequently  the  fact  that,  in  a 
continuous  rock  mass,  feldspar  is  most  completely  saussuritized  which 
occurs  in  the  least  crushed  portion,  while  the  rock  which  is  most  broken, 
stretched,  and  foliated  retains  its  feldspar  fragments  in  a quite  fresh 
and  unaltered  condition.  That  this  fresh  feldspar  is  not  a new  crys- 
tallization, is  proved  by  the  fact  that  fragments  can  often  be  seen  to 
have  once  fitted  together,  as  portions  of  one  individual,  before  the 
crushing  took  place.  Among  many  sections  in  which  this  phenomenon 
can  be  observed  may  be  mentioned  : The  Sturgeon  Falls  gabbro;  the 
rocks  of  the  diorite  ridge  near  the  Lower  Quinnesec  Falls ; Nos.  11004, 
11010,11019,  afid  11102  from  just  below  the  Lower  Quinnesec  Falls ; 
Nos.  11054,  11073,  and  11056  (see  Fig.  11)  from  Upper  Quinnesec  Falls; 
No.  11179  from  Four-Foot  Falls,  and  Nos.  11651  and  11652  from  the 
Cleveland  ore  dock  in  Marquette. 

Such  observations,  made  at  many  widely  separated  localities  within 
the  Menominee  and  Marquette  greenstone  areas,  would  at  first  thought 
seem  to  indicate  that  there  is  a reciprocal  relation  between  the  chemical 
and  mechanical  effects  produced  by  great  pressure.  In  other  words, 
that  the  force  which  in  the  m assive  portion  of  the  rock  caused  increased 
chemical  action  and  alteration  of  the  feldspar  to  saussurite,  was  ex- 
pended, in  another  part,  in  the  work  of  crushing.  The  fact,  however, 
that  the  bisilicate  constituents  are  more  altered  in  the  crushed  bands 
than  in  the  Other  part  of  the  rockmass  is  opposed  to  such  an  explana- 
tion, and  seems  rather  to  indicate  that  the  more  ready  alteration  of 
these  and  the  production  of  such  minerals  as  fibrous  hornblende,  chlorite, 
and  talc,  formed  a soft  matrix  which  protected  the  feldspar  from  the 
further  action  of  pressure  and  chemical  action. 

A totally  different  alteration  from  saussuritization  is  sometimes  ob- 
served in  the  feldspars  of  the  more  basic  eruptives.  This  consists  of 
their  change  to  green  hornblende  needles,  and  can  of  course  occur  only 
where  a portion  of  the  necessary  elements  is  furnished  by  some  bisili- 
cate. These  elements  (i.  e.,  magnesium  and  iron)  wander  along  the 
cleavage  cracks  of  the  feldspar,  causing  the  development  of  the  needles 
as  shown  in  PI.  XU,  fig.  2.  A very  complete  instance  of  this  change 
is  shown  in  the  epidiorite,  No.  11663,  from  Pine  street,  Marquette. 

Still  another  alteration  of  the  plagioclase  is  to  epidote.  This  is  com- 


216 


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[HULL..  62. 


plete  in  No.  11091  from  the  Horse  Race,  and  partial  in  No.  11712  from 
the  Brook  Section,  near  Marquette. 

While  the  lime  feldspars  change  to  zoisite,  epidote,  or  hornblende,  the 
alkaline  feldspars  show  a corresponding  tendency  to  pass  into  mica 
(sericite).  This  process  is  most  commonly  central,  the  periphery  of  a 
crystal  remaining  intact  after  the  interior  is  completely  altered,  as  may 
be  seen  in  No.  11104,  the  granite  from  south  of  Upper  Quinnesec  Falls. 
This  same  specimen  exhibits  an  interesting  phase  of  the  inverse  ratio 
existing  between  the  mechanical  and  the  chemical  action  in  the  acid 
feldspar.  Micro  dine  seems  to  have  been  abundantly  developed  from 
orthoclase  by  pressure  but  while  the  orthoelase  itself  is  sericitized,  the 
microcline  never  shows  a trace  of  this  change. 

Pyroxene  is  comparatively  rare  in  the  rocks  studied,  occurring  only 
as  diallage  in  the  Sturgeon  Falls  gabbro,  and  as  augite  in  the  younger 
Marquette  diabases $ nevertheless,  from  the  structure  of  many  of  the 
other  rocks,  we  may  affirm  with  certainty  that  they  once  contained  py- 
roxene, and  may  hence  trace  the  alterations  which  this  mineral  has  un- 
dergone. 

The  most  common,  and  indeed  the  almost  universal  change  of  the 
pyroxene  in  the  Menominee  and  Marquette  rocks  is  to  hornblende.  The 
compact  brown  hornblende  in  the  Sturgeon  Falls  gabbro  and  in  the 
porphyritic  rocks  from  the  west  end  of  the  ridge  near  Lower  Quinnesec 
Falls,  shows  strong  evidence  of  having  originated  from  pyroxene,  but 
this  can  not  perhaps  be  regarded  as  beyond  all  doubt.  Compact  green 
hornblende  appears  to  replace  original  diallage  in  the  gabbro-like 
diorite  which  forms  the  barrier  rock  at  Upper  Quinnesec  Falls  (see 
PI.  X,  fig.  1),  where  it  even  retains  the  orthopinacoidal  parting.  The 
same  mineral  likewise  seems  to  replace  original  augite  in  many  of  the 
Horse  Race  diorites,  whose  structure  is  typically  diabasic.  " 

Fibrous  green  hornblende  or  uralite  is  too  common  and  well  known 
an  alteration  product  of  pyroxene  to  deserve  especial  description.  It 
is  universally  distributed  through  all  of  the  more  basic  rocks  in  the 
areas  investigated. 

A colorless  chlorite  may  be  seen  originating  from  the  almost  color- 
less diallage  of  the  Sturgeon  Falls  gabbro,  as  shown  in  PI.  VIII,  fig. 
2.  From  the  varieties  of  pyroxene  which  are  richer  in  iron,  a deep  green 
chlorite  results  which  is  often  associated  with  epidote,  as  shown  in  PI. 
XI,  fig.  1. 

Hornblende. — Without  reference  to  the  original  or  secondary  origin  of 
the  hornblende  itself,  this  mineral  is  found  subject  to  several  different 
alterations. 

It  passes  from  the  compact  to  the  fibrous  form  by  fraying  out  at  the 
ends,  as  shown  in  specimen  No.  11175,  from  the  Four-Foot  Fall  (see 
Fig.  19,  p.  126).  It  also  seems  to  give  rise  to  biotite  in  many  of  the 
Horse  Race  diorites  and  in  the  amphibole  granite,  No.  11831,  obtained 
at  the  camp  northwest  of  Marquette.  (See  PI.  XVI.  fig.  2.)  Talc 


williams.]  BIOTITE,  OLIVINE,  AND  ILMENITE.  217 

frequently  is  produced  by  hornblende  alteration  in  the  Horse  Race 
diorites  as  described  in  Chap.  Ill  (p.  107).  A colorless  chlorite,  closely 
resembling  that  produced  from  the  Sturgeon  Falls  diallage,  is  derived 
from  the  pale  hornblende  (itself  probably  paramorphic)  of  No.  11098, 
from  the  ridge  near  Lower  Quinnesec  Falls.  This  is  produced  in  spots 
over  the  hornblende  and  is  visible  only  by  its  isotropic  behavior  in  polar- 
ized light,  as  shown  in  Fig.  9 (p.  79).  The  viridite  (chlorite)  epidote 
aggregate  originates  from  hornblende  just  as  it  does  from  pyroxene. 
Finally  serpentine  is  an  exceptional  result  of  hornblende  alteration,  as 
may  be  seen  in  specimens  11078  and  11191  from  the  Horse  Race  (p.  109). 

Biotite  shows  the  usual  alterations  and  is  principally  the  result 
of  weathering  rather  than  of  metamorphic  processes.  Bleaching  first 
takes  place  and  then  chloritization.  Carbonates  are  sometimes  sepa- 
rated in  the  form  of  interpolated  lenses,  while  the  titanium  which 
entered  into  their  composition  separates  out  sometimes  as  anatase 
(Nos.  11050  and  11052  from  Upper  Quinnesec  Falls)  and  sometimes  as 
rutile.1  (Nos.  11113,  from  near  Iron  Mountain  in  the  Menominee  valley, 
No.  11672  from  Marquette  and  No.  11738  from  the  Brook  Section.) 

Olivine  occurs  only  in  a few  of  the  Marquette  diabases,  where  its 
alteration  is  the  usual  one  to  serpentine. 

. Ilmenite  is  the  last  of  the  important  original  constituents  of  the 
Menominee  and  Marquette  massive  rocks  whose  alterations  can  be 
clearly  traced.  This  gives  rise  to  a variety  of  new  titanium  minerals 

Its  commonest  change  is  that  to  leucoxene,  which  is  everywhere 
encountered,  see  PI.  IX,  figs.  1 and  2. 

Sphene  or  titanite,  of  which  leucoxene  is  only  a special  form,  some- 
times originates  from  ilmenite,  as  is  shown  in  PI.  XIII,  fig.  1,  and  in 
PL  XVI,  fig.  2. 

Anatase  also,  in  association  with  leucoxene,  is  a secondary  product 
of  ilmenite  alteration.  This  is  shown  in  Fig.  25  (p.  131)  of  No.  11130, 
from  Twin  Falls,  as  well  as  in  No.  11802,  one  of  the  stretched  agglom- 
erates on  the  Carp  River.  (See  Chap.  Y,  p.  177.) 


'On  the  frequency  of  these  changes  see  Whitman  Cross:  “ Petrography  of  the  Leadville  Kocks” 
in  Mon.  U.  S.  Geol.  Survey,  vol.  12,  1887. 


PLATES. 


PLATE  VIII. 


PLATE  VIII. 


Fig.  1. — Saussurite  gabbro  ( first  stage). 

From  point  h,  PI.  Ill,  at  Sturgeon  Falls,  Menominee  River,  Michigan.  Specimen 
No.  11167a.  Ordinary  light.  (See  p.  68.) 

The  triclinic  feldspar,  which  shows  occasional  idiomorphic  forms  indicating  that 
it  is  in  part,  at  least,  older  than  the  pyroxene,  here  appears  almost  completely  altered 
to  an  opaque,  gray  saussurite.  A high  magnifying  power  resolves  this  into  an  aggre- 
gate of  minute  zoisite  needles,  calcite  and  albite.  These  are  somewhat  unevenly  dis, 
tributed  which  produces  the  blotched  appearance  of  the  saussurite.  , 

The  diallage,  which  is  of  a pale  green  color  in  the  hand-specimen,  is  almost  color- 
less when  seen  under  the  microscope.  Its  well  marked  orthopinacoidal  parting  is  seen 
on  the  right  of  the  figure.  This  diallage  is  surrounded  by  a border  of  compact  horn- 
blende, which  is  either  brown,  pale  green  or  colorless.  It  frequently  becomes  fibrous 
on’ its  exterior  edge,  as  is  shown  in  Fig.  7,  on  p.  70.  Small  patches  of  compact  brown 
hornblende  are  also  abundantly  scattered  over  the  entire  surface  of  the  diallage  in  a 
manner  that  would  seem  to  indicate  that  it  had  originated  from  the  latter  by  para- 
morphism.  There  is  some  pale  green  chlorite  visible  in  the  upper  part  of  the  draw- 
ing and  on  the  right  is  a bit  of  ilmenite  and  leucoxene. 

Fig.  2. — Saussurite  gabbro  ( second  stage). 

From  point  /,  PI.  Ill,  at  Sturgeon  Falls,  Menominee  River,  Michigan.  Specimen 
No.  11154.  Represented  between  crossed  nicol  prisms.  (Seep.  72.) 

A large  individual  of  the  pale  diallage  is  here  seen  in  an  advanced  stage  of  altera- 
tion to  a colorless  chlorite.  Because  of  the  almost  isotropic  character  of  this  mineral, 
it  is  necessary  to  show  its  appearance  in  polarized  light.  Imbedded  in  the  chlorite 
are  remnants  of  the  still  brightly  polarizing  diallage,  and  around  it  is  the  border  of 
hornblende,  which  here  shows  pale  yellow  interference  colors. 

The  feldspar  is  less  completely  saussuritized  than  in  the  last  figure.  Its  character- 
istic twinning  lamellae  are  still  visible  in  many  instances,  particularly  at  the  center 
of  the  crystals. 


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PLATE  IX. 

Fig.  1. — Altered  diabase  or  diorite. 

From  the  so-called  u Gabbro  Ridge, ” below  Lower  Quinnesec  Falls,  Menominee  River, 
Michigan.  Specimen  No.  11028.  Ordinary  light.  (Seep.  81. ) 

The  original  structure  of  this  rock  has  been  completely  changed,  in  spite  of  its  still 
massive  character.  It  is  now  composed  of  pale  green,  fibrous  hornblende,  saussurite, 
quartz,  calcite,  chlorite,  ilmenite,  and  leucoxene.  Most  of  these  constituents  are  of 
secondary  origin,  and  in  the  process  of  their  formation  the  form  of  the  primitive  min- 
erals has  been  so  completely  obliterated  that  it  is  now  impossible  to  say  whether  the 
mother-rock  was  a diabase  or  a diorite. 

Fig.  2. — Schistose  band  in  the  last  figured  rock,  showing  the  effect  of  dynamic  metamor- 
phism ( stretching ) upon  it. 

Locality  same  as  that  of  last  figure.  Specimen  No.  11031.  Ordinary  light.  (See 

p.  82.) 

The  feldspar  in  this  rock  is  chemically  less  altered  than  in  the  last,  but  it  has  been 
subjected  to  a much  more  intense  mechanical  action.  It  is  fractured,  aud  the  frag- 
ments are  widely  separated,  although  those  pieces  which  once  belonged  to  the  same 
crystal  may  still  often  be  identified.  The  interstices  are  filled  with  scales  of  a green 
chlorite,  arranged  parallel  to  one  another,  so  as  to  produce  a schistose  structure. 
Even  the  little  leucoxene  zones  around  the  ilmenite  grains  have  been  elongated  in 
the  same  direction. 


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PLATE  X. 


Fig.  1. — Saussurite  diorite. 

This  rock  forms  the  barrier  at  Upper  Quinnesec  Falls,  Menominee  River,  Michigan.  « 
Specimen  No.  11054.  Ordinary  light.  (See  p.  103.) 

In  spite  of  the  close  external  resemblance  of  this  rock  to  the  Sturgeon  Falls  saus-  I 
surite  gabbro  (PI.  VIII,  fig.  1),  it  shows  no  trace  of  any  pyroxenic  constituent.  Its  ; 
only  bisilicate  is  hornblende.  This  is  sometimes  compact  (and  then  both  brown  and 
green  in  color),  sometimes  ragged  and  fibrous.  The  former  variety  is  seen  in  the 
center  and  on  the  left  of  the  figure,  with  its  remarkably  perfect  orthopinacoidal  t 
parting,  like  that  recently  observed  by  Cathrein  in  a hornblende  from  Roda,  in  the 
Tyrol.  This  parting  may  be  an  indication  that  this  hornblende  has  been  derived 
* from  original  diallage.  A large  individual  of  the  more  ragged  and  fibrous  hornblende, 
filled  with  secondary  quartz,  is  shown  on  the  right  of  the  figure. 

The  feldspar  of  this  rock  has  undergone  the  usual  alteration  to  opaque,  gray  saus- 
surite, but  in  this  are  imbedded  frequent  grains  of  a fresh  brown  feldspar.  Leu-  . 
coxene  rims  around  the  ilmenite  are  abundant. 

Fig.  2. — Typical  aphanitic  greenstone  of  the  Marquette  region. 

From  Baldwin’s  Kilns,  northeast  of  Negaunee,  Michigan.  Specimen  No.  11747.  Or- 
dinary light.  (See  p.  172.) 

This  is  a fair  representative  of  the  commonest  rock  type  in  the  southern  Marquette 
and  Negaunee  greenstone  areas.  Its  grain  must  always  have  been  very  fine  and  com- 
pact. Long,  slender  feldspar  crystals  may  still  be  seen,  sometimes  with  an  imper- 
fectly developed  form,  such  as  is  common  in  the  semi-crystalline  rocks  (porphy rites),  i 
The  groundmass  is  composed  of  a fine  grained  aggregate  of  fibrous  hornblende, 
chlorite,  quartz,  calcite,  and  ilmenite  leucoxene.  These  minerals  are  all  secondary, 
and  may  easily  have  resulted  from  the  alteration  of  a cryptocrystalline,  or  even  a 
partially  vitreous  base. 

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Fig.  1 .-Chlorite-epidoie  aggregate  in  an  altered  diabase. 

From  below  Upper  Quinnesec  Falls,  Menominee  River,  Michigan.  Specimen  No. 

11049.  Ordinary  light.  (See  p.  97.) 

This  is  a very  common  alteration  product  in  rocks  of  the  diabase  type,  especially 
in  those  rich  in  iron.  In  a confused  mass  of  deep  green  and  somewhat  pleochroic* 
chlorite  scales  lie  embedded  extremely  sharp  crystals  of  a yellowish  or  colorless 
epidote.  These  latter  are  what  the  earlier  students  of  these  rocks  mistook  for! 
secondary  augite.  In  the  lower  part  of  the  figure  are  seen  ilmenite  grains  sur- 
rounded by  rims  of  leucoxene  and  a portion  of  a large  secondary  hornblende  crystal.) 

Fig.  2. — Stretched  greenstone. 

From  above  Lower  Quinnesec  Falls,  Menominee  River,  Michigan.  Specimen  No. 

11102.  Ordinary  light.  (Seep.  94.) 

The  effects  of  tension  upon  a solid  rock  mass  are  rarely  seen  more  distinctly  than 
in  this  specimen.  Not  only  the  feldspar,  but  also  a large  grain  of  ilmenite  has  here 
been  forcibly  torn  asunder,  and  the  fragments  have  been  separated  a considerable  dis- 
tance, always  in  one  direction.  The  peculiar  green  chlorite  so  characteristic  of  all 
stretched  basic  rocks  (cf.  PI.  IX,  fig.  2)  fills  the  interstices  between  the  mineral  frag- 
ments. It  must  have  crystallized  after  the  breaking  of  the  solid  rock  constituents 
and  its  scales,  which  are  all  arranged  parallel  to  the  direction  in  which  the  strain 
was  exerted,  produce  a decidedly  schistose  structure  in  the  rock.  The  fresh  state  oi 
the  feldspar  in  a rock  which  has  been  subjected  to  such  intense  mechanical  action  as 
this  one  is  very  noticeable. 

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Fig.  1. — Coarsely  crystalline  diorite. 

From  near  Baldwin's  Kilns,  northeast  of  Negaunee,  Michigan.  Specimen  No.  11749. 

Ordinary  light.  (See  p.  173.) 

This  one  of  the  coarse  grained  dike  rocks  which  penetrate  the  aphanitic  green- 
stones of  the  Negaunee  area.  The  hornblende  is  idiomorphic,  and,  as  there  are  no 
certain  traces  of  pyroxene,  the  rock  is  designated  a “ diorite.”  The  feldspar  is 
quite  filled  with  secondary  actinolite  or  epidote  needles.  The  hornblende  is  often 
altered  internally  to  chlorite  or  fibrous  amphibole,  while  its  exterior  still  remains 
compact  and  shows  a curious  concentration  of  the  green  coloring  matter.  There  is 
also  observable  around  the  edge  of  the  hornblende  crystals  a separation  into  fibers, 
as  described  by  Becke. 

Fig.  2. — Epidiorite. 

From  the  Horse  Race  above  Upper  Quinnesec  Falls,  Menominee  River,  Michigan. 

Specimen  No.  11186.  Ordinary  light.  (See  p.  107.) 

This  is  one  of  the  coarse  grained  dioritic  rocks  so  abundant  along  the  Horse  Race 
Rapid.  The  pale  green  hornblende  is  entirely  allotriomorphic  and  fills  the  spaces 
between  the  idiomorphic  feldspar  crystals  exactly  as  augite  does  in  diabase.  Still 
there  is  no  certain  trace  of  pyroxene  now  present.  The  hornblende  shows  a deeper 
color  around  its  edge  aDd  a breaking  up  into  fibers,  which  are  arranged  in  irregular 
bundles  and  appear  to  wander  off  into  the  surrounding  feldspar. 

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PLATE  XIII. 


Fig.  1. — Sphene  crystals  around  ilmenite. 

In  a dioritic  rock  from  the  Horse  Race  Eapid,  above  Upper  Quinnesec  Falls,  Meno- 
minee River,  Michigan.  Specimen  No.  11189.  Ordinary  light.  (See  p.  109.) 
These  sphene  crystals,  although  their  minerological  character  is  undoubted,  are 
not  so  clear  or  so  sharply  defined  as  usual.  They  are  gray  and  cloudy,  resembling 
leucoxene  in  appearance;  and,  like  this  substance  which  is  known  to  be  identical 
.with  sphene  in  its  composition,  these  crystals  surround  grains  of  iimenite,  as  though 
they  had  originated  from  its  alteration.  If  this  be  the  case,  we  have  here  an  inter- 
esting example  of  leucoxene  assuming  its  characteristic  titanite  form. 

Fig.  2. — Rutile  originating  from  the  alteration  of  ilmenite. 

In  a greenstone  from  below  the  Upper  Quinnesec  Falls,  Menominee  River,  Michigan. 
Specimen  No.  11070.  Ordinary  light.  (See  p.  99.) 

The  rock,  which  was  probable  once  a diabase,  now  consists  principally  of  green 
chlorite  and  reddish  feldspar  substance.  The  opaque  iron  oxide  now  present  is 
magnetite.  This  occupies  irregular  areas  and  is  intimately  associated  with  a net- 
work of  yellow  rutile  needles  in  a manner  which  renders  probable  the  origin  of  both 
of  these  minerals  from  an  original  ilmenite. 

232 


U. S. GEOLOGICAL  SURVEY 


BULLETIN  No  62  PLATE  XIII. 


FIG. I (XQO) 


FIG  2 IXIIOI 

G H W DEL 


THE  LIBRARY 
OF  THE 


PLATE  XI Y 


PLATE  XIV. 


Fig.  1. — Sericite  porphyry. 

From  just  below  the  Upper  Quinnesec  Falls,  Menominee  River,  Wisconsin.  Specimen 
No.  11050.  Nicols  crossed.  (Seep. 121.) 

This  rock,  which  was  once  an  eruptive  quartz  porphyry,  shows  in  an  admirable 
manner  the  effect  of  stretching.  The  porphyritic  quartz  crystals  are  somewhat 
elongated  and  testify  to  the  tension  to  which  they  have  been  subjected  by  an  undu- 
latory  extinction.  The  porphyritic  feldspar  crystals  are  fractured  and  pulled  apart 
always  in  the  same  direction,  without  reference  to  the  position  which  they  thern- 
selwes  occupied  in  the  rock.  The  fissures  are  cemented  by  a new  crystallization  of 
sericite.  The  microgranitic  groundmass  has  been  rendered  schistose  by  stretching  and 
by  the  abundant  production  of  sericite,  whose  scales  have  a parallel  arrangement. 

Fig.  2. — Stretched  and  hrecciated  greenstone. 

From  near  the  Carp  River,  north  of  Teal  Lake,  Michigan.  Specimen  11803.  Nicols 

crossed.  (Seep. 177.) 

Some  of  the  interstitial  material,  occurring  between  the  massive  cores  of  the 
spheroidally  parted  (hrecciated)  greenstones,  contains  distinct  crystals  of  white 
feldspar.  Between  the  eastern  end  of  Teal  Lake  and  the  Carp  River  some  of  these 
massive  cores  are  themselves  much  elongated  by  stretching.  (See  Fig.  27,  p.177.)  A 
section  of  the  insterstitial  material  from  this  locality  was  selected  for  illustration  be- 
cause of  the  distinctness  Avith  which  this  stretching  is  apparent  in  the  feldspar 
crystals.  They  are  always  broken  and  pulled  apart  in  the  same  direction,  while  the 
smaller  components  of  the  rock  show  a corresponding  elongation.  The  continuity  of 
the  original  rock-structure  in  the  interstitial  portion  of  this  exposure  indicates  that 
the  spheroidal  parting  is  in  this  case  a result  of  cooling,  rather  than  of  mechanical 
brecciation  in  situ.  (See  p.  167.) 

234 


U.S. GEOLOGICAL  SURVEY. 


BULLETIN  No.  62  PLATE  XIV. 


FIG. I (X30) 


FIG. 2 ( X30) 


G.  H.W  DEI. 


the  UBRMK 
Of THE 

USIVERSITY  OF  ILUIOB 


PLATE  XV. 


PLATE  XV. 


Fig.  1. — Structure  of  one  of  the  11  Augen”  in  an  “Augengneiss,”  or  stretched  granite  por- 

phyry. 

From  a schistose  dike  in  the  greenstones  of  the  Horse  Race  Rapid  above  Upper  Quin- 
nesec  Falls,  Menominee  River,  Michigan.  Specimen  No.  11184.  Ordinary  light. 
(Seep.  118.) 

The  center  of  the  “Auge,”  or  eye,  is  seen  to  consist  of  a portion  of  an  old,  brown 
colored  porphyritic  feldspar  crystal.  This  is  granulated  on  either  side,  and  pulled 
out  into  a lens,  whose  longest  axis  agrees  with  the  direction  of  the  foliation.  The 
granulation  is  composed  of  a new  crystallization  of  the  feldspar  substance,  which  is 
clear,  and  although  granitic  in  structure,  it  has  a much  coarser  grain  than  the  rest 
of  the  rock.  This  formation  of  an  “Auge”  out  of  a porphyritic  feldspar  crystal 
agrpes  with  the  observations  of  J.  Lehmann,  Chelius,  and  others. 

Fig.  2. — Stretched  quartz  porphyry . 

From  a conformable  dike  in  the  schistose  greenstones  of  the  Brook  Section,  west  of 
Marquette,  Mich.  Specimen  No.  11707.  Nicols  crossed.  (Seep.  150.) 

This  rock  is  particularly  noticeable  on  account  of  the  wonderful  manner  in  which 
it  shows  the  effects  of  a stretching  action  upon  quartz.  The  original  crystals  are 
elongated  into  lenticular  and  pear  shaped  forms,  or  even  into  long,  narrow  bands. 
The  first  effect  of  the  tension  is  to  disturb  the  optical  homogeneity  and  produce  an 
undulatory  extinction.  If,  however,  the  strain  is  great  enough  to  overcome  the  force 
of  cohesion,  a mosaic  of  interlocking  and  differently  orientated  grains  is  the  result. 
Similar  phenomena  have  been  observed  and  illustrated  by  J.  Lehmann  in  Saxony. 
The  porphyritic  feldspar  crystals  in  this  rock  are.  not  broken,  nor  do  they  show  the 
evidence  of  great  pressure.  Their  form  is  generally  intact,  but  it  is  worthy  of  re- 
mark that  their  center  is  always  occupied  by  an  irregular  area  of  microcline. 

The  groundmass  is  finely  microgranitic,  containing  sinuous  bands  of  micaceous 
minerals,  which  bend  around  the  porphyritic  constituents,  while  they  follow  the 
general  direction  of  the  foliation. 

236 


U S. GEOLOGICAL  SURVEY. 


BULLETIN  No.  62  PLATE  XV. 


FIG.  I ( X30) 


FIG. 2 ( X30) 


H.W  DEL 


THE  LIBRARY 
OF  THE 

UNIVERSITY  OF  ILLINOIS 


PLATE  XVI. 


237 


PLATE  XVI. 


Fig.  1. — Greenstone  schist  (tuff)  of  the  northern  Marquette  area. 

Lighthouse  Point,  Marquette,  Mich.  Specimen  No.  11619.  Ordinary  light.  (See 
p.  155.) 

A characteristic,  although  by  no  means  universal  structure,  in  the  banded  green 
schists  which  compose  so  large  a portion  of  the  region  around  Marquette,  consists  in 
the  tufted  form  of  the  hornblende  crystals.  These,  although  quite  compact  at  their 
centers,  are  fibrous  at  the  ends  and  expand  so  as  to  resemble  sheaves  tied  in  the  mid- 
dle. The  fibers  are  so  fine  and  the  radial  arrangement  at  the  ends  of  the  bundles  is 
so  perfect  that  the  arm  of  a black  cross  is  seen  to  sweep  across  the  field  when  the 
thin  section  is  viewed  between  crossed  nicol-prisms.  Hornblende  with  a structure 
like  this  has  been  observed  by  Renard  and  others"  as  a new  crystallization  in  altered 
sediments,  a fact  which  lends  additional  support  to  the  hypothesis  that  these  green 
schists  are  tuff  deposits. 

# 

Fig.  2. — Amphibole  granite  (?)  forming  a dike  in  aplianitic  greenstones. 

Northeast  of  Negaunee,  Mich.  Specimen  No.  11831.  Ordinary  light  in  part ; polar- 
ized light  in  part.  (See  p.  181.) 

This  rock  presents  many  points  of  interest,  both  in  its  structure  and  alteration 
products.  The  feldspar  is  in  two  distinct  generations,  of  which  the  older  variety  is 
entirely  idiomorphic,  with  a zone  of  clear  substance  surrounding  a gray  and  more 
altered  interior. 

The  hornblende  exhibits  the  unusual  alteration  to  biotite,  which  is  sometimes 
brown,  sometimes  green.  This  mineral  in  rare  instances  has  crystallized  in  sharp 
hexagonal  plates  which  show  pressure  lines  of  cleavage  (“  Drucklinien  ”). 

The  groundmass  of  this  rock  is  an  aggregate  of  quartz  and  the  younger  generation 
of  feldspar.  These  sometimes  form  a microgranitic  mosaic  and  sometimes  micro- 
pegmatitic  growths,  which  are  represented  in  the  figure  as  they  appear  in  polarized 
light.  Apatite  is  abundant,  and  also  ilmenite  or  magnetite  surrounded  by  chlorite, 
and  in  some  cases  by  sphene,  as  though  this  had  resulted  from  the  alteration  of  tfie 
ilmenite,  as  shown  in  PI.  XIII,  fig.  1. 

238 


U S. GEOLOGICAL  SURVEY. 


BULLETIN  No.  62  PLATE  XVI 


FIG. I 1X30) 


FI  G.  2 ( X30) 


G H.W  DEL 


THE  LIBRARY 
OF  THE 

UNIVERSITY  OF  ILLIHOtS 


INDEX 


Page. 

Acid  rocks,  eruptive,  origin  of 123 

Actinolite 108, 181 

Adinole 152 

Agglom  erates 187 

Albite  . . 69,209 

Albite  mosaic 60, 156,  210 

. Allanite  (see  orthite) 118 

Amphibole  granite 181 

Amygdaloidal  structure 174 

Analyses  ... .76, 89,  91, 104, 113, 119, 120, 121, 152, 153 

Anatase 63, 121, 131, 177,  212,  217 

Andesine 114 

Apatite 200 

Aphanitic  greenstones 163, 171 

Augengneiss 118,207 

Augen  structure 75, 118,  207 

Augen  in  banded  greenstone  schists 157 

Augite 139, 175, 200 


B- 


Bald win’s  Kilns 

Baltzer,  A.  cited 

Banded  greenstone  schists 

Bayley,  Prof.  W.  S.. 

Becko,  Fr.,  cited 

Becker,  G.  F 

Biotite 

after  hornblende 

Bonney,  T.  G 

Brogger,  'W'.  C.,  cited 

Brook  Section 

Brooks,  Maj.  T.  B 


172,178 

44, 47 

154,184 

14, 32 

126,173 

57 

107,108,  200,  212,217 

182 

46 


42,  63 

143 

17,  25,  65, 110, 124 


C. 


Calcite  in  granites 114, 122 

Carbonates - 214 

Carbonatization 36 

Carp  River 175 

Catbrein,  A.,  cited 59,  63,  69, 100, 103 

Chelius,  C.,  cited 50 

Chlorite 55,213 

Chlorite,  colorless 73,  79, 105 

Chlorite  produced  by  stretching 83, 164, 

171,176,208 

Chlorite-epidoto  aggregate 56,  90,  97, 214 

Cliloritization 55 

Clay  slate 124 

Cleveland  ore  dock,  Marquette '58 

Compression 202 


Page. 

j Cores,  massive  in  schist 93 

Credner,  H.,  cited 25,  64, 102, 119 

Cross,  W.,  cited 167 

Cross-gashes  (Klaffende  Risse) 80.  92,  204 

Crushing 214 


D. 


Dana,  J.  D.,  cited 61 

Datbe,  cited 57 

DaubrCe,  cited 44 

Dead  River,  Falls  of 180 

Deer  Lake,  agglomerates  of 185 

Diabase 138, 183, 197 

glassy 140, 143, 198 

micropegmatitic.. 141 

olivine 138, 143, 180 

tuffs  of 133,158 

Diabase  Porphyry 198 

Diallage 70,  87, 200, 206 

Diller,  J.  S , cited 131, 153 

Diorite 146,181,197 

Diorite  Porphyry 199 

j Dutton,  C.  E.,  cited , 159 

E. 

| Epidiorite 131, 144, 145 

j Epidote  (after  feldspar) 108, 211 

Epidotization 56 

j Euroka  Series,  Marquette 137 

F. 


Feldspar 214 

| brown. 103,105,108 

J clear  periphery  of 79, 90, 103, 108 

deformation  of 48, 205 

freshest  where  crushed 72,  82,  88, 93, 103, 

105, 169, 215 

zonal 117, 148, 178 

| Felsite 122 

I Flaser  structure 75,  87, 119, 203 

; Foliation  from  join  ting 128 

from  shearing 129, 142 

Foster  and  'Whitney,  cited 15,  25 

Four-Foot  Falls 123 

G. 

Gabbro 197 

olivine 180, 197 

saussunte 67, 170 

33<J 


240 


INDEX, 


Page.  ] 

Gabbro-diorite 86 

“ Gabbro  Ridge  ” of  Brooks 77  I 

Garnet 108,210 

Geikie,  A.,  cited 153, 161, 190 


Gneiss 122 

Granite 111,147,178,199 

Granite  gneiss : 113, 115, 116  j 

Granite  porphyry 117,199 

Granulation,  peripheral  ..  .48, 112, 117, 147, 148,  207 

Great  Dyke,  Marquette 138 

Groddeck,  A.  von.,  cited 62  | 


H. 


Hagge,  cited 58 

Harrington  B , cited 53 

Heim,  A.,  cited 43,  47 

Helminth 55,  71 

Hitchcock,  E.,  cited 162 

Hornblende 206 

brown 77,  79, 200 

like  diallage  102 

surround. ng  diallage 70 

sheaf-like 155 

secondary  to  compact  brown 

hornblende  after  pyroxene 72  78  87,  211 

fibrous,  not  a secondary  enlarge- 
ment  105, 126, 173,  210 

with  granulated  center 145 

changing  to  chlorite 79 

changing  to  serpentine 109,170 

Horse  Race  Rapid 96. 106 


I. 


Ilmenite 200 

altered  to  sphene 109,217 

stretching  of 95,  206 

probable  change  of,  to  rutile  and  mag- 
netite   99-101 

InostranzefF,  cited 54 

Irving,  R.  D 185 

views  of,  regarding  the  Marquette  re- 
gion   19-24 

views  of,  regarding  the  Menominee 
region 29-30,  67 


J. 


M. 


Magnetite 

Marquette. 

Melaphyre 

Metamorphism,  defined 
macro-structural. . . 

micro-structural 

mineralogieal 

Mica 

Microcline 

Microflaser  structure  . . 

Micropegmatite 

Mortar  structure 

Muscovite 


Page. 

200 

134 

198 

36 

43,202 

46,205 

50, 208 

206 

.111,199, 210,  216 
..75, 117,170, 176 

141,182 

48, 207 

117,199,212 


N. 


Naumann,  C.  F.,  cited 167 

Eegaunee  area 171 

Novaculite 151,179 


O. 


Oligoclase 

Olivine 

Olivine  diabase  . . 

Olivine  gabro 

Ophitic  structure 
Orthite 


111,199 

180,  200,  217 

138, 143, 180 

197 

196 

117, 118, 178,  200 


Orthoclase 199 

Orthopinacoid  parting  in  hornblende 103 


Parting,  orthopinacoidal 70, 103 

rhomboidal 128 

spheroidal 137, 166, 20,3 

Penfield,  S.  L.,  cited 100 

Phillip  s,  J.  A. , cited 161 

Picnic  Islands,  Marquette 146, 198 

Poicilitic  structure 78,  79, 183, 196 

Porphyroids 119 

Pseudo-porphyritic  structure 207 

• Pnmpelly,  R.,  cited 67 

Pyroxene 206 

alterations  of 216 

change  of  to  hornblende  not  simple 

paramorphism 52 


Jointing 

Judd,  J.  W.,  cited  . 
Julien,  A.  A.,  cited 


K. 


Kimhall,  J.  P.,  cited 
Kloos,  J. H.,  cited  ... 


L. 


128 
39,  50 
146 


i6 

53 


Q. 


Quartz 

broken 

deformation  of 

Quartz  porphyry 

Quartzite 

Quinnesec,  Lower  Falls 
Upper  Falls 


199,210 

112 

48, 117, 148, 150,  205 

148,199 

179 

77 

96 


Labradorite 104, 199 

Laspeyres,  cited 61 

Lawson,  A.  C.,  cited 12, 136, 162, 166, 178 

Lehmann,  J.,  cited 45,  47, 48, 59, 62, 118, 150 

Leucoxene 63, 83 

Lossen,  K.  A.,  cited 38, 41, 42,  49,  59, 152, 161 

Lower  Quinnesec  Falls 77 


R. 


Reusch,  H.  H.,  cited 44,  46, 161 

Rhomboidal  parting  in  greenstones 83 

Rominger 18, 19, 27, 06 

Rosenbuscli 49,  52. 55 

Ro  hpletz,  A.,  cited 44, 168 


INDEX. 

241 

Rutile 

(thonschiefernadeln) 

after  biotite 

after  ilmenite 

Page. 

84,91,212 

98,106,212 

115,124,178 

99-101 

Tuffs  of  diabase 

| acid  rocks 

Carp  River 

Deer  Lake 

Twin  Falls 

Page. 

133,  184, 199 

151 

177  8 

185 

127 

s. 


Saussurite 

Saussurite  gabbro 

Saussuritization 

Schalstein 

Schenck,  A.,  cited 

Schistose  porphyry 

Schmidt,  C.,  cited 

Seri  cite  

Sericite  schists 

Sericitization  

Serpentine  after  hornblende 

Shearing 

Sphene .' 

after  ilmenite 

Spheroidal  parting 

Stelzner,  cited 

Stretching,  effects  of 

Sturgeon  Falls 


59,103,210  | 
67  ! 


54,56 

119 

46, 62 

61,121,212 

74,  84,  88, 105 

60 

.109,170,  214 

129,130,203 

111,200,212,217 

109,182 

137, 166,  203 

121 

...82,  94,177,188,  204 
67 


T. 


Talc 107, 214 

Teal  Lake 175 

Teall,  J.  J.  H. , cited  46,  53 

Thonschiefernadeln  (see  rutile) 98, 106,  212 

Titanic  iron  (see  ilmenite) 200 

Tornebohm,  A.  E.,  cited  48 


Tourmaline Ill,  112, 114, 124,  200,  206 


U. 


Upper  Quinnesec  Falls 96 

Upper  Twin  Falls  132 

Uralite 52 

double  zone  of,  around  pyroxene 142 

Uralite  diabase 174,175 

Uralitization 52 


V. 


Yan  Hise,  C.  R.,  cited 

Variolite  (?) 

Viridite .. .. 

Vogelsand,  H.,  cited. . 


W. 


,70,105, 126, 173 

173 

56,  97 

34 


Wadsworth,  M.  E.,  cited 17,  5p,  51, 146, 150, 154 

Weathering  defined  36 

Weiss,  C.  E.,  cited  46,49,150,195 

Whotstone,  see  novaculite. 

Whetstone  brook,  Marquette 164 

Wichmann,  cited 57,  65,  90,  123 

Wright,  C.E 26,123 


Z. 


Zircon  ...  Ill,  113, 122, 124,  200, 206 

Zoisite 69, 102, 184,  210 


Title  for  subject  entry.  Author  title.  Series  title. 


LIBRARY  CATALOGUE  SLIPS. 


United  States.  Department  of  the  interior.  ( XJ.  S.  geological  survey). 

Department  of  the  interior  J — | Bulletin  | of  the  | United 
States  j geological  survey  | no.  63  | [Seal  of  the  department]  | 

Washington  | government  printing  office  | 1890 

Second  title:  United  States  geological  survey  | J.  W.  Powell, 
director  | — | A bibliography  | of  | paleozoic  Crustacea  | from  | 
1698  to  1889  | including  a list  of  north  american  species  and  a | 
systematic  arrangement  of  genera  | by  | Anthony  W.  Vogdes  ] 
[Vignette]  | 

Washington  | government  printing  office  j 1890 

8°.  177  pp. 


Vogdes  (Anthony  Wayne). 

United  States  geological  survey  | J.  W.  Powell,  director  | — | 
A bibliography  | of  | paleozoic  Crustacea  | from  | .1698  to  1889  | 
including  a list  of  north  american  species  and  a | systematic  ar- 
rangement of  genera  | by  | Anthony  W.  Vogdes  | [Vignette]  | 
Washington  | government  printing  office  | 1890 
8°.  177  pp. 

[United  States.  Department  of  the  interior.  ( TJ . S.  geological  survey). 

Bulletin  63] . 


United  States  geological  survey  | J.  W.  Powell,  director  | — | 
A bibliography  | of  | paleozoic  Crustacea  | from  | 1698  to  1889  | 
including  a list  of  north  american  species  and  a | systematic  ar- 
rangement of  genera  | by  | Anthony  W.  Vogdes  | [Vignette]  | 
Washington  | government  printing  office  | 1890 
6°.  177  pp. 

[United  States.  Department  of  the  interior.  (TJ.  S.  geological  survey). 

Bulletin  63]. 


ADVERTISEMENT. 


[Bulletin  No.  63.1 


The  publications  of  the  United  States  Geological  Survey  are  issued  in  accordance  with  the  statute 
approved  March  3,  1879,  which  declares  that — 

• ‘ The  publications  ofthe  Geological  Survey  shall  consist  of  the  annual  report  of  operations,  geological 
and  economic  maps  illustrating  the  resources  and  classification  of  the  lands,  and  reports  upon  general 
and  economic  geology  and  paleontology.  The  annual  report  of  operations  of  the  Geological  Survey 
shall  accompany  the  annual  report  of  the  Secretary  of  the  Interior.  All  special  memoirs  and  reports 
of  said  Survey  shall  he  issued  in  uniform  quarto  series  if  deemed  necessary  by  the  Director,  but  other- 
wise in  ordinary  octavos.  Three  thousand  copies  of  each  shall  be  published  for  scientific  exchanges 
and  for  sale  at  the  price  of  publication ; and  all  literary  and  cartographic  materials  received  in  exchange 
shall  be  the  property  of  the  United  States  and  form  a part  of  the  library  of  the  organization : And  the 
money  resulting  from  the  sale  of  such  publications  shall  be  covered  into  the  Treasury  of  the  United 
States.” 

On  July  7,  1882,  the  following  joint  resolution,  referring  to  all  Government  publications,  was  passed 
by  Congress: 

1 ‘ That  whenever  any  document  or  report  shall  be  ordered  printed  by  Congress,  there  shall  be  printed, 
in  addition  to  the  number  in  each  case  stated,  the ‘usual  number’  (1,900)  of  copies  for  binding  and 
distribution  among  those  entitled  to  receive  them.” 

Except  in  those  cases  in  which  an  extra  number  of  any  publication  has  been  supplied  to  the  Survey 
by  special  resolution  of  Congress  or  has  been  ordered  by  the  Secretary  of  the  Interior,  this  office  has 
no  copies  for  gratuitous  distribution. 

ANNUAL  REPORTS. 

I.  First  Annual  Report  of  the  United  States  Geological  Survey,  by  Clarence  King.  1880.  8°.  79  pp. 
1 map.— A preliminary  report  describing  plan  of  organization  aud  publications. 

II.  Second  Annual  Report  of  the  United  States  Geological  Survey,  1880- ’81,  by  J.  W.  Powell.  1882. 
8°.  lv,  588  pp.  62  pi.  1 map. 

III.  Third  Annual  Report  of  the  United  States  Geological  Survey,  1881-’82,  by  J.  W.  Powell.  1883, 
8°.  xviii,  564  pp.  67  pi.  and  maps. 

IV.  Fourth  Annual  Report  of  the  United  States  Geological  Survey,  1882-83,  by  J.  W.  Powell.  1884. 
8°.  xxxii,  473  pp.  85  pi.  and  maps. 

V.  Fifth  Annual  Report  of  the  United  States  Geological  Survey,  1883-’84,  by  J.  W.  Powell.  1885i 
8°.  xxxvi,  469  pp.  58  pi.  and  maps. 

VI.  Sixth  Annual  Report  of  the  United  States  Geological  Survey,  1884-’85,  by  J.  W.  Powell.  1885. 
8°.  xxix,  570  pp.  65  pi.  and  maps. 

VII.  Seventh  Annual  Report  of  the  United  States  Geological  Survey,  1885-’86,  by  J.  W.  Powell.  1888. 
8°.  xx,  656  pp.  71  pi.  and  maps. 

VIII.  Eighth  Annual  Report  of  the  United  States  Geological  Survey,  1886-87,  by  J.  W.  Powell.  1889. 
8°.  2 v.  xix,  474,  xii  pp.  53  pi.  and  maps ; 1 p.  1. 475-1063  pp.  54-76  pi.  and  maps. 

IX.  Ninth  Annual  Report  of  the  United  States  Geological  Survey,  1887-88,  by  J.  W.  Powell.  1890. 
8°.  xiii,  717  pp.  88  pi.  and  maps. 

The  Tenth  Annual  Report  is  in  press. 

MONOGRAPHS. 

I.  Lake  Bonneville,  by  Grove  Karl  Gilbert.  1890.  4°.  xx,  438  pp.  51  pi.  1 map.  Price  $1.50. 

II.  Tertiary  History  ofthe  Grand  Canon  District,  with  atlas,  by  Clarence  E.  Dutton,  Capt.  U.  S.  A. 
1882.  4°.  xiv,  264  pp.  42  pi.  and  atlas  of  24  sheets  folio.  Price  $10.12. 

III.  Geology  of  the  Comstock  Lode  and  the  Washoe  District,  with  atlas,  by  George  F.  Becker.  1882. 
4°.  xv,  422  pp.  7 pi.  and  atlas  of  21  sheets  folio.  Price  $11.00. 

IV.  Comstock  Mining  and  Miners,  by  Eliot  Lord.  1883.  4°.  xiv,  451  pp.  3 pi.  Price  $1.50. 

V.  The  Copper-Bearing  Rocks  of  Lake  Superior,  by  Roland  Duer  Irving.  1883.  4°.  xvi,  464  pp. 
15  1.  29  pi.  and  maps.  Price  $1.85. 

VI.  Contributions  to  the  Knowledge  of  the  Older  Mesozoic  Flora  of  Virginia,  by  William  Morris 
Fontaine.  1883.  4°.  xi,  144  pp.  54  1.  54  pi.  Price  $1.05. 


I 


II  ADVERTISEMENT. 


VII.  Silver- Lead  Deposits  of  Eureka,  Nevada,  by  Joseph  Story  Curtis.  1884.  4°.  xiii,  200  pp.  16 
pi.  Price  $1.20. 

VM.  Paleontology  of  the  Eureka  District,  by  Charles  Doolittle  Walcott.  1884.  4°.  xiii,  298  pp. 
241.  24  pi.  Price  $1.10. 

IX.  Brachiopoda  and  Lamellibranchiata  of  the  Raritan  Clays  and  Greensand  Marls  of  New  Jersey, 
by  Robert  P.  Whitfield.  1885.  4°.  xx,  338  pp.  35  pi.  1 map.  Price  $1.15. 

X.  Dinocerata.  A Monograph  of  an  Extinct  Order  of  Gigantic  Mammals,  by  Othniel  Charles  Marsh. 
1886.  4°.  xviii,  243  pp.  561.  56  pi.  Price  $2.70. 

XI.  Geological  History  of  Lake  Lahontan,  a Quaternary  Lake  of  Northwestern  Nevada,  by  Israel 
Cook  Russell.  1885.  4°.  xiv,  288  pp.  46  pi.  and  maps.  Price  $1.75. 

XII.  Geology  and  Mining  Industry  of  Leadville,  Colorado,  with  atlas,  by  Samuel  Franklin  Emmons. 
1886.  4°.  xxix,  770  pp.  45  pi.  and  atlas  of  35  sheets  folio.  Price  $8.40. 

XIII.  Geology  of  the  Quicksilver  Deposits  of  the  Pacific  Slope,  with  atlas,  by  George  F.  Becker. 
1888.  4°.  xix,  486  pp.  7 pi.  and  atlas  of  14  sheets  folio.  Price  $2.00. 

XIV.  Fossil  Fishes  and  Fossil  Plants  of  the  Triassic  Rocks  of  New  Jersey  and  the  Connecticut  Val- 
ley. by  John  S.  Newberry.  1888.  4°.  xiv,  152  pp.  26  pi.  Price  $1.00. 

XV.  The  Potomac  or  Younger  Mesozoic  Flora,  by  William  Morris  Fontaine.  1889.  4°.  xiv,  377 
pp.  180  pi.  Text  and  plates  bound  separately.  Price  $2.50. 

XVI.  The  Paleozoic  Fishes  of  North  America,  by  John  Strong  Newberry.  1889.  4°.  340  pp.  53  pi. 
Price  $1.00. 

In  preparation  : 

— Gasteropoda  of  the  New  Jersey  Cretaceous  and  Eocene  Maris,  by  R.  P.  Whitfield. 

— The  Penokee  Iron-Bearing  Series  of  Northern  Wisconsin  and  Michigan,  by  Roland  D.  Irving  and 
C.  R.  Van  Hise. 

— Mollusca  and  Crustacea  of  the  Miocene  Formations  of  New  Jersey,  by  R.  P.  Whitfield. 

— Description  of  New  Fossil  Plants  from  the  Dakota  Group,  by  Leo  Lesquereux. 

— Geology  of  the  Eureka  Mining  District,  Nevada,  with  atlas,  by  Arnold  Hague. 

— Sauropoda,  by  O.  C.  Marsh. 

— Stegosauria,  by  O.  C.  Marsh. 

— Broqfotheridae,  by  O.  C.  Marsh. 

— Report  on  the  Denver  Coal  Basin,  by  S.  F.  Emmons. 

— Report  on  Silver  Cliff  and  Ten-Mile  Mining  Districts,  Colorado,  by  S.  F.  Emmons. 

— Flora  of  the  Dakota  Group,  by  J.  S.  Newberry. 

— The  Glacial  Lake  Agassiz,  by  Warren  Upham. 

— Geology  of  the  Potomac  Formation  in  Virginia,  by  W.  M.  Fontaine. 


BULLETINS. 


1.  On  Hypersthene-Andesite  and  on  Triclinic  Pyroxene  in  Augitic  Rocks,  by  Whitman  Cross,  witn  a 
Geological  Sketch  of  Buffalo  Peaks,  Colorado,  by  S.  F.  Emmons.  1883.  8°.  42pp.  2 pi.  Price  10  cents. 

2.  Gold  and  Silver  Conversion  Tables,  giving  the  coining  values  of  troy  ounces  of  fine  metal,  etc.,  com- 
puted by  Albert  Williams,  jr.  1883.  8°.  8 pp.  Price  5 cents. 

3.  On  the  Fossil  Faunas  of  the  Upper  Devonian,  along  the  meridian  of  76°  30',  from  Tompkins  County, 
N.  Y.,  to  Bradford  County,  Pa.,  by  Henry  S.  Williams.  1884.  8°.  36  pp.  Price  5 cents. 

4.  On  Mesozoic  Fossils,  by  Charles  A.  White.  1884.  8°.  36  pp.  9 pi.  Price  5 cents. 

5.  A Dictionary  of  Altitudes  in  the  United  States,  compiled  by  Henry  Gannett.  1884.  8°.  325  pp. 
Price  20  cents. 

6.  Elevations  in  the  Dominion  of  Canada,  by  J.  W.  Spencer.  1884.  8°.  43  pp.  Price  5 cents. 

7.  Mapoteca  Geologica  Americana.  A Catalogue  of  Geological  Maps  of  America  (North  and  South), 
1752-1881,  in  geographic  and  chronologic  order,  by  Jules  Marcou  and  John  Belknap  Marcou.  1884. 
8°.  184  pp.  Price  10  cents. 

8.  On  Secondary  Enlargements  of  Mineral  Fragments  in  Certain  Rocks,  by  R.  D.  Irving  and  C.  R. 
Van  Hise.  1884.  8°.  56  pp.  6 pi.  Price  10  cents. 

9.  AReportof  work  donein  the  Washington  Laboratory  during  the  fiscal  year  1883-’84.  F.  W.  Clarke, 
ihief  chemist.  T.  M.  Chatard,  assistant  chemist.  1884.  8°.  40  pp.  Price  5 cents. 

*10.  On  the  Cambrian  Faunas  of  North  America.  Preliminary  studies,  by  Charles  Doolittle  Walcott. 
1884.  8°.  74  pp.  10  pi.  Price  5 cents. 

11.  On  the  Quaternary  and  Recent  Mollusca  of  the  Great  Basin ; with  Descriptions  of  New  Forms,  by 
R.  Ellsworth  Call.  Introduced  by  a sketch  of  the  Quaternary  Lakes  of  the  Great  Basin,  by  G.  K. 
Gilbert.  1884.  8°.  66  pp.  6 pi.  Price  5 cents.  • 

12.  A Crystallographic  Study  of  the  Thinolite  of  Lake  Lahontan,  by  Edward  S.  Dana.  1884.  8?. 
34  pp.  3 pi.  Price  5 cents. 

13.  Boundaries  of  the  United  States  and  of  the  several  States  and  Territories,  with  a Historical 
Sketch  of  the  Territorial  Changes,  by  Henry  Gannett.  1885.  8°.  135  pp.  Price  10  cents. 

14.  The  Electrical  and  Magnetic  Properties  of  the  Iron-Carburets,  by  Carl  Barus  and  Vincent 
Strouhal.  1885.  8°.  238  pp.  Price  15  cents. 

15.  On  the  Mesozoic  and  Cenozoic  Paleontology  of  California,  by  Charles  A.  White.  1885.  8°. 
33  pp.  Price  5 cents. 


ADVERTISEMENT. 


Ill 


16.  On  the  Higher  Devonian  Faunas  of  Ontario  County,  New  York,  by  John  M.  Clarke.  1885.  8°. 
86  pp.  3 pi.  Price  5 cents. 

17.  On  the  Development  of  Crystallization  in  the  Igneous  Rocks  of  Washoe,  Nevada,  with  Notes  on 
the  Geology  of  the  District,  by  Arnold  Hague  and  Joseph  P.  Hidings.  1885.  8°.  44  pp.  Price  5 cents. 

18.  On  Marine  Eocene,  Fresh- water  Miocene,  and  other  Fossil  Mollusca  of  Western  North  America, 
by  Charles  A.  White.  1885.  8°.  26  pp.  3 pi.  Price  5 cents. 

19.  Notes  on  the  Stratigraphy  of  California,  by  George  F.  Becker.  1885.  8°.  28  pp.  Price  5 cents. 

20.  Contributions  to  the  Mineralogy  of  the  Rocky  Mountains,  by  Whitman  Cross  and  W.  F.  Hille- 
brand.  1885.  8°.  114  pp.  1 pi.  Price  10  cents. 

21.  The  Lignites  of  the  Great  Sioux  Reservation.  A Report  on  the  Region  be  tween  the  Grand  and  Mo- 
reau Rivers,  Dakota,  by  Bailey  Willis.  1885.  8°.  16  pp.  5 pi.  Price  5 cents. 

22.  On  New  Cretaceous  Fossils  from  California,  by  Charles  A.  White.  1885.  8°.  25  pp:  5 pi.  Price 
5 cents. 

23.  Observations  on  the  Junction  between  the  Eastern  Sandstone  and  the  Keweenaw  Series  on 

Keweenaw  Point,  Lake  Superior,  by  R.  D.  Irving  and  T.  C.  Chamberlin.  1885.  8°.  124  pp.  17  pi. 

Price  15  cents. 

24.  List  of  Marine  Mollusca,  comprising  the  Quaternary  Fossils  and  recent  forms  from  American 
Localities  between  Cape  Hatteras  and  Cape  Roque,  including  the  Bermudas,  by  William  Healey  Dali. 
1885.  8°.  336  pp.  Price  25  cents. 

25.  The  Present  Technical  Condition  of  the  Steel  Industry  of  the  United  States,  by  Phineas  Barnes. 
1885.  8°.  85  pp.  Price  10  cents. 

26.  Copper  Smelting,  by  Henry  M.  Howe.  1885.  8°.  107  pp.  Price  10  cents.  . 

27.  Report  of  work  done  in  the  Division  of  Chemistry  and  Physics,  mainly  during  the  fiscal  year 

1884-  85.  1886.  8°.  80  pp.  Price  10  cents. 

28.  The  Gabbros  and  Associated  Hornblende  Rocks  occurring  in  the  Neighborhood  of  Baltimore,  Md., 
by  George  Huntington  Williams.  1886.  8°.  78  pp.  4 pi.  Price  10  cents. 

29.  On  the  Fresh-water  Invertebrates  of  the  North  American  Jurassic,  by  Charles  A.  White.  1886. 
Ip.  41  pp.  4 pi.  Price  5 cents. 

30.  Second  Contribution  to  the  Studies  on  the  Cambrian  Faunas  of  North  America,  by  Charles  Doo- 
little Walcott.  1886.  8°.  369  pp.  33  pi.  Price  25  cents. 

31.  Systematic  Review  of  our  Present  Knowledge  of  Fossil  Insects,  including  Myriapods  and  Arach- 
nids, by  Samuel  Hubbard  Scudder.  1886.  8°.  128  pp.  Price  15  cents. 

32.  Lists  and  Analyses  of  the  Mineral  Springs  of  the  United  States;  a Preliminary  Study,  by  Albert 
C.  Peale.  1886.  8°.  235  pp.  Price  20  cents. 

33.  Notes  on  the  Geology  of  Northern  California,  by  J.  S.  Diller.  1886.  8°.  23  pp.  Price  5 cents. 

34.  On  the  relation  of  the  Laramie  Molluscan  Fauna  to  that  of  the  succeeding  Fresh-water  Eocene 
and  other  groups,  by  Charles  A.  White.  1886.  8°.  54  pp.  5 pi.  Price  10  cents. 

35.  Physical  Properties  of  the  Iron-Carburets,  by  Carl  Barus  and  Vincent  Strouhal.  1886.  8°.  62 
pp.  Price  10  cents. 

36.  Subsidence  of  Fine  Solid  Particles  in  Liquids,  by  Carl  Barus.  1886.  8°.  58  pp.  Price  10  cents. 

37.  Types  of  the  Laramie  Flora,  by  Lester  F.  Ward.  1887.  8°.  354 yjp.  57  pi.  Price  25  cents. 

38.  Peridotite  of  Elliott  County,  Kentucky,  by  J.  S.  Diller.  1887.  8°.  31  pp.  1 pi.  Price  5 cents. 

39.  The  Upper  Beaches  and  Deltas  of  the  Glacial  Lake  Agassiz,  by  Warren  Upham.  1887.  8°.  84 
pp.  1 pi.  Price  10  cents. 

40.  Changes  in  River  Courses  in  Washington  Territory  due  to  Glaciation,  by  Bailey  Willis.  1887.  8°. 
10  pp.  4 pi.  Price  5 cents. 

41.  On  the  Fossil  Faunas  of  the  Upper  Devonian — the  Genesee  Section,  New  York,  by  Henry  S. 
Williams.  1887.  8°.  121  pp.  4 pi.  Price  15  cents. 

42.  Report  of  work  done  in  the  Division  of  Chemistry  and  Physics,  mainly  during  the  fiscal  year 

1885- ’86.  F.  W.  Clarke,  chief  chemist.  1887.  8°.  152  pp.  1 pi.  Price  15  cents. 

43.  Tertiary  and  Cretaceous  Strata  of  the  Tuscaloosa,  Tombigbee,  and  Alabama  Rivers,  by  Eugene 
A.  Smith  and  Lawrence  C.  Johnson.  1887.  8°.  189  pp.  21  pi.  Price  15  cents. 

44.  Bibliography  of  North  American  Geology  for  1886,  by  Nelson  H.  Darton.  1887.  8°.  35  pp. 
Price  5 cents. 

45.  The  Present  Condition  of  Knowledge  of  the  Geology  of  Texas,  by  Robert  T.  Hill.  1887.  8°.  94 
pp.  Price  10  cents. 

46.  Nature  and  Origin  of  Deposits  of  Phosphate  of  Lime,  by  R.  A.  F.  Penrose,  jr.,  with  an  Introduc- 
tion by  N.  S.  Shaler.  1888.  8°.  143  pp.  Price  15  cents. 

47.  Analyses  of  Waters  of  the  Yellowstone  National  Park,  with  an  Account  of  the  Methods  of  Anal- 
syis  employed,  by  Frank  Austin  Gooch  and  James* Edward  Whitfield.  1888.  8°.  84  pp.  Price  10 

cents. 

48.  On  the  Form  and  Position  of  the  Sea  Level,  by  Robert  Simpson  Woodward.  1888.  8°.  88  pp. 

Price  10  cents. 

49.  Latitudes  and  Longitudes  of  Certain  Points  in  Missouri,  Kansas,  and  New  Mexico,  by  Robert 
Simpson  Woodward.  1889.  8°.  133  pp.  Price  15  cents. 

50.  Formulas  and  Tables  to  facilitate  the  Construction  and  Use  of  Maps,  by  Robert  Simpson  Wood- 
ward. 1889.  8°.  124  pp.  Price  15  cents. 


IV 


ADVERTISEMENT. 


51.  On  Invertebrate  Fossils  from  the  Pacific  Coast,  by  Charles  Abiathar  "White.  1889.  8°.  102  pp. 

14  pi.  Price  15  cents. 

52.  Subaerial  Decay  of  Hocks  and  Origin  of  the  Red  Color  of  Certain  Formations,  by  Israel  Cook 
Russell.  1889.  8°.  65  pp.  5 pi.  Price  10  cents. 

53.  The  Geology  of  Nantucket,  by  Nathaniel  Southgate  Shaler.  1889.  8°.  55  pp.  10  pi.  Price  10 
cents. 

54.  On  the  Thermo-Electric  Measurement  of  High  Temperatures,  by  Carl  Barus.  1889.  8°.  313  pp. 
incl.  1 pi.  11  pi.  Price  25  cents. 

55.  Report  of  work  done  in  the  Division  of  Chemistry  and  Physics,  mainly  during  the  fiscal  year 

1886- ’87.  Frank  Wigglesworth  Clarke,  chief  chemist.  1889.  8°.  96  pp.  Price  10  cents. 

56.  Fossil  Wood  and  Lignite  of  the  Potomac  Formation,  by  Frank  Hall  Em owlton.  1889.  8°.  72  pp. 
7 pi.  Price  10  cents. 

57.  A Geological  Reconnaissance  in  Southwestern  Kansas,  by  Robert  Hay.  1890.  8°.  49  pp.  2 pi. 
Price  5 cents. 

58.  The  Glacial  Boundary  in  Western  Pennsylvania,  Ohio,  Kentucky,  Indiana,  and  Illinois,  by  George 
Frederick  Wright,  with  an  introduction  by  Thomas  Chrowder  Chamberlin.  1890.  8°.  112  pp.  incl. 
1 pi.  8 pi.  Price  15  cents. 

59.  The  Gabbros  and  Associated  Rocks  in  Delaware,  by  Frederick  D.  Chester.  1890.  8°.  45  pp. 
1 pi.  Price  10  cents. 

60.  Report  of  work  done  in  the  Division  of  Chemistry  and  Physics,  mainly  during  the  fiscal  year 

1887- 88.  F.  W.  Clarke,  chief  chemist.  1890.  8°.  174  pp.  Price  15  cents. 

61.  Contributions  to  the  Mineralogy  of  the  Pacific  Coast,  by  William  Harlow  Melville  and  Waldemar 
Lindgren.  1890.  8°.  40  pp.  3 pi.  Price  5 cents. 

63.  A Bibliography  of  Paleozoic  Crustacea  from  1698  to  1889,  including  a list  of  North  American 
species  and  a systematic  arrangement  of  genera,  by  Anthony  W.  Yogdes.  1890.  8°.  177  pp.  Price 

15  cents. 

64.  A Report  of  work  done  in  the  Division  of  Chemistry  and  Physics,  mainly  during  the  fiscal  ^ear 

1888- ’89.  F.  W.  Clarke,  chief  chemist.  1890.  8°.  60  pp.  Price  10  cents. 

66.  On  a Group  of  Volcanic  Rocks  from  the  Tewan  Mountains,  New  Mexico,  and  on  the  occurrence 
of  Primary  Quartz  in  certain  Basalts,  by  Joseph  Paxson  Hidings.  1890.  8°.  34  pp.  Price  5 cents. 
In  press: 

62.  The  Greenstone  Schist  Areas  of  the  Menominee  and  Marquette  Regions  of  Michigan,  by  George 
H.  Williams;  with  an  Introduction  by  R.  D.  Irving. 

65.  Comparative  Stratigraphy  of  the  Bituminous  Coal  Rocks  of  the  Northern  Half  of  the  Appala- 
chian Field,  by  I.  C.  White. 

67.  On  the  relations  of  the  Traps  of  the  Newark  System  in  the  New  Jersey  Region,  by  Nelson  H. 
Darton. 

In  preparation : 

— Natural  Gas  Districts  in  Indiana,  by  Arthur  John  Phinney. 

— A Classed  and  Annotated  Bibliography  of  Fossil  Insects,  by  Samuel  Hubbard  Scudder. 

— The  Viscosity  of  Solids,  by  Carl  Barus. 

— Mesozoic  Fossils  in  the  Permian  of  Texas,  by  C.  A.  White. 

— A Late  Volcanic  Eruption  in  Northern  California  and  its  Peculiar  Lava,  by  J.  S.  Diller. 

— Altitudes  between  Lake  Superior  and  the  Rocky  Mountains,  by  Warren  Upham. 

STATISTICAL  PAPERS. 

Mineral  Resources  of  the  United  States,  1882,  by  Albert  Williams,  jr.  1883.  9°.  xvii,  813  pp.  Price 
50  cents. 

Mineral  Resources  of  the  United  States,  1883  and  1884,  by  Albert  Williams,  jr.  1885.  8°.  xiv,  1016 
pp.  Price  60  cents. 

Mineral  Resources  of  the  United  States,  1885.  Division  of  Mining  Statistics  and  Technology.  1886. 
8°.  vii,  576  pp.  Price  40  cents. 

Mineral  Resources  of  the  United  States,  1886,  by  David  T.  Day.  1887.  8°.  viii,  813  pp.  Price  50 
cents. 

Mineral  Resources  of  the  United  States,  1887,  by  David  T.  Day.  1888.  8°.  vii,  832  pp.  Price  50 
cents. 

Mineral  Resources  of  the  United  States,  1888,  by  David  T.  Day.  1890.  8°.  vii,  653  pp.  Price  50 
cents. 

The  money  received  from  the  sale  of  these  publications  is  deposited  in  the  Treasury,  and  the  Secre- 
tary of  that  Department  declines  to  receive  bank  checks,  drafts,  or  postage  stamps : all  remittances, 
therefore,  must  be  by  postal  note  or  money  okder.  made  payable  to  the  Librarian  of  the  U.  S.  Geo- 
logical Survey,  or  in  currency,  for  the  exact  amount.  Correspondence  relating  to  the  publications  of 
the  Survey  should  be  addressed 

To  the  Director  of  the 

United  States  Geological  Survey, 

Washington,  D.  C. 

Washington,  D.  C.,  August,  1890. 


DEPARTMENT  OF  THE  INTERIOR 


BULLETIN 


OF  THE 

UNITED  STATES 

* 

GEOLOGICAL  SURVEY 


NTo.  63 


WASHINGTON 
GOVERNMENT  PRINTING  OFFICE 
1890 


UNITED  STATES  GEOLOGICAL  SURVEY 

J.  W.  POWELL,  DIRECTOR 


A BIBLIOGRAPHY 

OF 

PALEOZOIC  CKITSTACEA 

FROM 

1698  to  1889 

INCLUDING  A LIST  OF  NORTH  AMERICAN  SPECIES  AND  A 
SYSTEMATIC  ARRANGEMENT  OF  GENERA 

BY 

ANTHONY  W.  VOGDES 


WASHINGTON 

GOVERNMENT  PRINTING  OFFICE 
1890 


‘ CONTENTS. 


Letter  of  transmittal 

Introduction 

I.  List  of  authors 11 

II.  Catalogue  of  trilobites 79 

III.  Catalogue  of  non-trilobites 149 

5 


Department  of  the  Interior, 

United  States  Geological  Survey, 
Division  of  Paleozoic  Invertebrate  Paleontology, 

Washington,  D.  G.,  May  1,  1890. 


LETTER  OF  TRANSMITTAL. 


Sir:  I have  the  honor  to  transmit  herewith,  for  publication,  a bibli- 
ography of  Paleozoic  Crustacea,  prepared  by  Lieutenant  A.  W.  Vogdes, 


The  bibliography  bears  internal  evidence  of  long  continued  and  ex- 
tended research  and  its  publication  will  supply  a work  of  reference 
that  has  long  been  needed  by  the  student  of  invertebrate  Paleozoic 
fossils. 

I remain,  very  respectfully, 


U.  S.  A. 


Chas.  D.  Walcott, 

Paleontologist. 


Hon.  J.  W.  Powell, 

Director  U . 8.  Geological  Survey. 


INTRODUCTION. 


The  sole  object  of  this  bulletin  is  to  give  a general  view  of  the  litera- 
ture on  the  Paleozoic  Crustacea  and  to  aid  students  and  paleontologists 
in  their  researches.  It  is  the  result  of  more  or  less  constant  work 
during  the  past  ten  years. 

In  its  compilation  I have  examined  almost  every  reference  before  re- 
cording it;  those  not  so  examined  are  indicated  by  a star  (*)  follow- 
ing the  title. 

For  convenience,  the  subject-matter  has  been  arranged  as  follows: 

Part  I.  List  of  authors,  including  a brief  index  of  the  genera  de- 
scribed in  each  work. 

Part  II.  A catalogue  of  the  North  American  Paleozoic  trilobites. 

Part  III.  The  non-trilobitic  Paleozoic  Crustacea,  with  a list  of  the 
species. 

I am  well  aware  that  the  value  of  a work  of  this  kind  depends  upon 
the  care  and  labor  given  to  its  compilation.  Every  possible  means  of 
obtaining  accurate  information  from  a miscellaneous  class  of  literature 
in  many  languages  has  been  used,  and  it  is  hoped  that  there  are  but 
few  errors  and  omissions. 

I would  thank  those  into  whose  hands  this  bulletin  may  fall  for  any 
information  that  would  add  to  its  value  as  a working  hand-book, 

A.  W.  Vogdes. 

Fort  Hamilton,  New  York  Harbor,  April  30, 1889. 


9 


PART  I. 


LIST  OF  AUTHORS. 


A BIBLIOGRAPHY  OF  PALEOZOIC  CRUSTACEA  FROM  1698  TO  1889, 

INCLUDING 

A LIST  OP  NORTH  AMERICAN  SPECIES  AND  A SYSTEMATIC  ARRANGEMENT  OP  GENERA. 


By  Anthony  W.  Vogdes. 

PART  I. 

LIST  OF  AUTHORS. 

A star  (*)  following  a title  indicates  that  the  reference  is  recorded  without  opportunity  for  personal 


verification. 

Agassiz  (L.)  Monographic  des  poissons 
fossiles  du  vieux  gres  rouge  oil  systeme 
d6vonien  (old  Red  Sandstone)  des  lies 
Britanniques  et  de  Russie. 

Text,  Soleure;  atlas,  Neuch&tel,  1845,  pp. 
xix-xx,  notd;  and  atlas,  Tab.  A. 

Pterygotus  n.  g. 

Alth  (Alois  von).  Ueber  die  palaeozoi- 
schen  Gebilde  Podoliens  und  deren  Ver- 
steinerungen.  Erste  Abtheilung. 

In  Abhandl.  k.  k.  geol.  Reichsanst.,  vol.  7, 
pt.  1,  Wien,  1874,  5 pi. 

Proetus , Gyphaspis,  Dalmania , Calymene, 
Ceraurus , Sphcerexochus,  Encrinurus , lllcenus, 
Eurypterus,  Pterygotus,  Stylonurus,  Beyrichia, 
Leperditia,  Primitia,  Bairdia. 

Alton  (Ed.  de).  See  Burmeister  and 
Alton. 

Ami  (Henry  M. ) Notes  on  Triarthrus 
8pino8M  Billings. 

In  Trans.  Ottawa  Field  Nat.  Club,  No.  4, 
18i*2-'83,  p.  88,  1 pi. 

Angelin  (N.  P.)  Palseontologia  Scandi- 
navica.  Pars  I.  Crustacea  formationis 
transitionis.  Lipsite,  1854,  4to. 

The  first  part  of  this  work,  entitled  “Palae- 
ontologia  Scandinavica,”  containing  pp.  1-24  and 
pi.  1-24,  was  published  by  the  Royal  Swedish 
Academy  of  Sciences  in  1852.  The  second  por- 
tion in  1854,  including  a preface,  pp.  1-9  and  pp. 
21-92,  pi.  25-42. 

The  genera  are  arranged  in  the  following 
order:  Olenus,  Paradoxides,  Gryptonynus,  Eryx  | 


Angelin  (N.  P.) — Continued. 

n.  g.  (corrected  by  Angelin  to  Elyx,  the  ge- 
neric term  Eryx  having  been  used  by  Stephen 
in  1832  for  a genus  of  the  Coleoptera),  Acontheus 
n.  g.  (corrected  by  the  author  to  that  of  Aneu- 
canthus),  Agnostus,  Phacops,  Polytomurus , Re- 
mopleurides,  Niobe  n.  g.,  Megalaspis  n.  g.,  Nileus, 
Ampyx,  Proetus,  Plicethonides  (Angelin  uses  this 
term  for  that  of  Phaeton  Barr.),  Forbes-ia,  Gonio- 
pleura,  Celmus  n.  g.,  Anomocare  n.  g.,  Soleno- 
pleura  n.  g.,  Liostracus  n.  g.,  Calymene,  Homa- 
lonotus,  Pliomera  ( Amphion ),  Cheirurus,  Cyrto- 
metopus  n.  g.,  Acidaspis,  Trapelocera,  Sphce- 
rexochus, Acidaspis,  Rhodope  n.  g.  (this  term 
was  used  by  Siebold  in  1848  for  a genus  of  the 
Gasteropoda),  Dysplanus,  Bumastus,  lllcenus, 
JEglina,  Olenus , Peltura,  Parabolina,  Acerocare 
n.  g.,  Leptoplastus  n.  g.,  Eurycare  n.  g.  (this 
genus  is  referred  by  J.  W.  Salter,  Mem.  Geol. 
Survey  United  Kingdom,  Brit.  Organic  Re- 
mains, decade  xi,  pi.  8,  p.  3,  to  the  genus  Splice - 
rophthalmus  Ang.),  Sphcerophthalmus  n.  g., 
Anopocare  n.  g.  (this  genus  is  referred  by  J.  G.  O. 
Linnarsson,  Geol.  Fbrening.  Stockholm  Forhdl., 
vol.  5, 1880— ’81,  p.  136,  to  the  genera  Peltura  and 
Sphcerophthalmus;  the  specimen,  according  to 
Dr.  Linnarsson, in  the  Royal  Museum  of  Swollen, 
“marked  by  Angelin  as  the  abdomen  till  Stenom. 
pusillus,  contains  several  small  heads  of  Sphce- 
rophthalmus alatus,  and  a small  pygidium  of 
Peltura  scarabceoides Dr.  Linnarsson  refers  to 
this  specimen  as  Angelin’s  typo  for  the  genus 
Anopocare  and  also  remarks  “that  Angelin  in- 
tended to  change  the  family  name  of  Sphceroph- 
thalmu8  alatus  and  their  nearest  forms  to  that 
of  Stenometopus,  inasmuch  as  another  speci- 
men of  Sph.  alatus  has,  in  Angelin’s  own  hand- 

13 


14 


A BIBLIOGRAPHY  OF  PALEOZOIC  CRUSTACEA. 


[BULL.  63. 


Angelin  (N.  P.) — Continued. 

writing,  the  generic  name  of  Stenometopus"), 
Ptychopyge  n.  g.,  Asaphus,  Bronteus,  Holome- 
topu8  n.  g.,  Isocolus,  Corynexochus  n.  g.,  Sym- 
physurus,  Euloma  n.  g.,  Pharostoma , Cono- 
coryphe.  Trinucleus,  Sphcerexocoryphe  n.  g.,  Dei- 
phon,  Staurocephalus , Lichas,  Dolichometopus 
n.  g.,  Platymetopus,  Cyrtometopus,  Ampyx, 
Jlaphiophorus,  Lonchodomas,  Harpes , Arraphus 
n.  g.,  Harpides,  Centropleura  n.  g.  (J.  G.  O.  Lin- 
narsson,  Svenska  Yetensk.  Akad.  Handl.,  vol.  8, 
1869,  No.  2,  p.  71,  cites  Angelin’s  Centropleura 
angusticauda  and  C.  dicrceura  under  Dr.  Owen’s 
genus  Dikelocephalus) , Cybele,  Telephus,  Ogygia , 
Ogygiocaris  n.  g. 

Palseontologia  Scandinavica.  Pars  I. 

Crustacea  formationis  transitionis  fas- 
ciculi 1 et  2 cum  tabulis  48.  Holmiae, 
1878  (3d  ed.). 

This  work  contains  plates  1,  la,  2,  3,  20,  22, 
with  an  appendix,  pp.  93-96.  Emended  and  re- 
vised by  Prof.  Gustaf  Lindstrdm. 

The  appendix  contains  descriptions  and  fig- 
ures of  the  following  species:  Paradoxides  tes- 
sini,  P.  tessini  var.  wahlenbergii,  P.  tessini  var. 
celandicus,  P.  affinis,  P.  tuber culatus,  P.  forch- 
hammeri,  P.  tumidus,  Centropleura  loveni,  C. 
steenstmpi,  Ogygiocaris  dilatata,  O.  dilatata 
var.  sarsi,  0.  dilatata  var.  str'omi,  in  addition 
to  the  genera  and  species  described  in  the 
second  edition. 

Anthony  (J.  G.)  New  Trilobites. 

In  Am.  Jour.  Sci.,  1st  series,  vol.  34,  1838,  p. 
379. 

Ceratocephala  ceralepta,  figs.  1 and  2. 

Description  of  a new  fossil  {Calymene 

bucklandii). 

In  Am.  Jour.  Sci.,  1st  series,  vol.  36,  1839,  p. 
106. 

In  this  article  a specimen  of  Ceraurus  pleur- 
exanthemus  Green  was  figured  and  described 
under  the  name  of  Calymene  bucklandii  as  a 
new  species. 

Audouin  ( J.  Y. ) Recherches  sur  les 
rapports  uaturels  qui  existent  entre  les 
Trilobites  et  les  animaux  articul^s. 

In  Annales  G6n.  Sc.  Phys.  Nat.,  Bruxelles, 
vol.  8, 1821,  pi.  18,  p.  233  ; also  Isis  (Oder  Encyc. 
Zeitung),  Oken,  vol.  1,  1822,  p.  87. 

Calymene  blumenbachii. 

Baily  (W.  H.)  On  two  new  species  of 
Crustacea  ( Belinurus  Kiinig)  from  the 
Coal  Measures  in  Queen’s  County,  Ire- 
land ; and  some  remarks  on  forms  allied 
to  them. 

In  Rept.  28th  Meeting  Brit.  Assoc.  Adv.  Sci., 
1858,  p.  76. 

On  the  annuloid  Crustacea  of  the 

Coal  Measures.  (*) 

In  Jour.  Geol.  Soc.  Dublin,  vol.  8,  1858,  p.  89. 

In  this  paper  a description  of  a fossil  Crusta-  I 


Baily  (W.  H.) — Continued. 

cean  from  the  Rilboa  Colliery,  Queen’s  County, 
was  given,  with  a few  remarks  on  the  allied 
species  from  Coal  Brook  Dale,  which  had  been 
included  with  it  in  the  genus  Limulus,  and  it 
was  proposed  to  remove  all  these  Coal-Measure 
Crustacea  from  that  genus  and  group  them 
into  a new  one,  under  the  name  of  Steropis. 

Remarks  on  some  Coal-Measure  Crus- 
tacea belonging  to  the  genus  Belinurus 
Kdnig,  with  descriptions  of  two  new 
species  from  Queen’s  County,  Ireland. 
PI.  5. 

In  Annals  Nat.  Hist.,  3d  series,  vol.  2, 1863,  p. 
105.  Translated  by  Milne- Edwards,  Annales 
G6n.  Sc.  Phys.  Nat.,  Bruxelles,  1863. 

The  author  herein  describes  Belinurus  re • 
gin.ce , B.  arcuatus , B.  bellulus,  B.  rotundus  ? 

Charles  Konig  in  his  work  (leones  Fos- 
silium  Sectiles,  London,  1825)  simply  mentions 
the  name  of  Belinurus  bellulus  in  his  explana- 
tion of  pi.  18,  fig.  230. 

Figures  of  characteristic  British  fos- 
sils, with  descriptive  remarks. 

Pt.  1,  pis.  1-10,  Cambrian  and  Lower  Silu- 
rian, London,  1867;  pt.  2,  pis.  11-20,  1869;  pt. 
3,  pis.  21-30,  1871. 

Paradoxides,  Dikelocephalus? , Olenus,  Palceo- 
pyge,  Conocoryphe , Angelina , Proetus , Phacops, 
Calymene,  Homalonotus,  Lichas , Trinucleus, 
Ampyx , Asaphus,  Ogygia,  Niobe,  Psilocephalus, 
ASglina,  Cheirurus , Sphcerexochus,  Encrinurus, 
Illoenus , Agnostus,  Eurypterus , Pterygolus, 
Ceratiocaris,  Beyrichia,  Cythere,  Primitia, 
Hymenocaris. 

On  Trilobites  and  other  fossils  from 

Lower  or  Cambro-Silurian  strata  in  the 
county  of  Clare.  (*) 

In  Jour.  Royal  Geol.  Soc.  Ireland,  vol.  17,  pt. 
1,  1886,  p.  29. 

Banks  (R.  W.)  On  the  tilestones  or- 
Downton  sandstones,  in  the  neighbor- 
hood of  Kington,  and  their  contents. 

In  Quart.  Jour.  Geol.  Soc.  London,  vol.  12, 
1856,  p.  93,  plate. 

Pterygotus,  Pteraspis,  Eurypterus,  Hunan- 
top  ter  us. 

Barrande  (Joachim).  Notice  pr61imi- 
naire  sur  le  systkme  silurien  et  les  Tri- 
lobites de  Boberne.  Leipsic,  1846. 

Etage  C : Paradoxides,  Conocephalus,  Ellipso- 
cephalus , Arion  n.  g.,  Sao  n.  g.,  Baltus,  Hydro- 
cephalus n.  g.,  Monadina  n.  g. 

Etage  D : Phacops,  Calymene,  Odontopleura, 
Asaphus,  Cheirurus,  Trinucleus , Caphyra  n g., 
Dione  n.  g.,  Illcenus,  Egle  n.  g.,  Battus. 

Etage  E : Phacops,  Arethusa  n.  g.,  Sphcerexo- 
chus, Asaphus,  Cheirurus,  Calymene,  Stauro- 
cephalus n.g.,  Lichas,  Harpes,  Odontopleura , 
Cyphaspi8,  Bronteus , Phceton  n.  g.,  Proetus. 


VODGES.] 


LIST  OF  AUTHORS. 


15 


Barrande  (Joachim) — Continued. 

32tage  F : Phacops,  Bronteus,  Lidias,  Proetus, 
Harpes,  Cheirurus,  Odontopleura,  Cyphaspis. 

35  tage  G : Phacops , Bronteus,  Cheirurus,  Cy- 
phaspis, Odontopleura,  Proetus.  % 

Nouveaux  Trilobites.  Supplement  h 

la  Notice  prdliminaire  sur  le  syst&me 
silurien  et  lea  Trilobites  de  Boheme. 
Prague,  1846. 

Etage  C : Schistes  fossiliferes. 

Etage  D : Cheirurus,  Phacops,  Ampyx,  Gdon- 
topleura,  lllcenus. 

Etage  E:  Arethusa,  Harpes. 

Etage  F : Proetus,  Phceton,  Bronteus,  Odon- 
topleura. 

Etage  G : Harpes,  Cheirurus,  Phacops. 

UeberdasHypostomaundEpistoma, 

zwei  analoge  aber  verschiedene  Organe 
der  Trilobiten. 

In  Neues  Jahrbucli  fur  Mineral.,  1847,  p.  885, 
pi.  8. 

Phacops  sodalis,  P.  breviceps,  Amphion,  II- 
Icenus,  Cheirurus,  Asaphus,  Lichas. 

The  generic  term  Dione  is  herein  modified  to 
that  of  Dionide,  p.  391. 

Sao  hirsuta  Barrande,  ein  Bruch- 

stuck  aus  dem  “Syst&me  silurien  du 
centre  de  la  Boheme.” 

In  Neues  Jahrhuch  fiir  Mineral.,  1849,  p.  385, 
pi.  7. 

Sao. 

Note  on  Trilobites. 

In  Ber.  Mittheil.  Freunde  Naturw.,  "Wien, 
vol.  4,  1849,  p.  353. 

Noticed  by  J.  "W.  Salter. 

In  Quart.  Jour.  Geol.  Soc.  London,  vol,  6, 1849, 
pt.  2,  p.  34. 

Deiphon  forbesii , neuer  Trilobit  aus 

Bohmen. 

In  Ber.  Mittheil.  Freunde  Naturw.,  "Wien, 
vol.  5,  1850,  p.  6. 

Versuch  einer  Klassification  der  Tri- 
lobiten. 

In  Neues  Jahrhuch  fiir  Mineral.,  1850,  p.  769. 

Syst&me  silurien  du  centre  de  la 

Boheme.  lre  partie.  Recherches  pald- 
ontologiques.  Prague  et  Paris,  1852. 

Yol.  1.  Text,  Crustac6s,  Trilobites.  With 
atlas  of  51  pis. 

This  classical  work  contains  a historical 
sketch  of  all  the  genera  of  Trilobites,  and  de- 
scriptions of  the  following  genera: 

Harpes,  Remoplcurides,  Paradoxides,  Hydro- 
cephalus, Sao,  Arionellus  n.  g.,  Ellipsocephalus, 
Olenus,  Peltura,  Triarthrus,  Conocephalites, 
Proetus,  Phillipsia,  Griffithides,  Cyphaspis,  Are- 
thusina  (generic  term  changed  from  that  of 
Arethus  to  Arethusina),  Harpides,  Phacops, 
Dalmanites,  Calymene,  Homalonotus,  Lichas, 
Trinucleus,  Ampyx,  Dionide  (generic  term 


Barrande  (Joachim)— Continued. 

changed  from  Dione  to  Dionide),  Asaphus, 
Ogygia,  Mglina  n.  g.,  lllcenus,  Nileus,  Sym- 
physurus,  Acidaspis,  Cheirurus,  Placoparia, 
Sphcerexochus,  Staurocephalus,  Deiphon,  Dindy- 
mene,  Zethus,  Amphion . Encrinurus,  Cromus 
n.  g.,  Bronteus,  Agnostus,  Telephus  n.  g. 

On  Ceratiocaris  bohemicus. 

In  Neues  Jahrhuch  fiir  Mineral.,  1853,  pt.  3, 
pp.  335-347. 

On  p.  335  of  this  article  there  is  a review  of 
Dr.  D.  D.  Owen’s  Kept.  Geol.  Survey  Wiscon- 
sin, Iowa,  and  Minnesota,  Phila.,  1852. 

? Dicalocephalus , etc. 

— — Note  sur  quelques  nouveaux  fossiles 
ddcouverts  aux  environs  de  la  ville  de 
Rokitzan  dans  le  bassin  silurien  du 
centre  de  la  Boheme. 

In  Bull.  Soc.  G6ol.  France,  2d  series,  vol.  13, 
1856,  p.  532. 

Calymene.  Placoparia,  Acidaspis,  Agnostus, 
Amphyx,  Harpes,  Ogygia. 

Mere  mention  of  locality  and  period. 

Wiedererscheinung  der  Gattung^Ire- 

thusina  Barrande. 

In  Neues  Jahrhuch  fiir  Mineral.,  1858,  p.  257, 

1 pi. 

Arethusina  sandbergeri  Barr. 

Documents  anciens  et  nouveaux  sur 

la  faune  primordiale  et  le  SystSme 
Taconique  en  Amdrique. 

In  Bull.  Soc.  G6ol.  France,  2d  series,  vol.  18, 
1861,  pp.  203-321,  pis.  4, 5. 

Paradoxides  asaphoides  Emmons,  P.  thomp- 
soni  Hall,  P.  macrocephalus  Emmons,  P.  ver- 
montana  Hall,  Peltura  ( Olenus ) holopyga  Hall, 
Atops  trilineatus  Emmons,  A.  punctatus  Em- 
mons, Triarthrus  bedci  Green,  Microdiscus 
quadrico status  Emmons. 

I.  Rdapparition  du  genera  Arethu- 
sina Barrande.  II.  Faune  silurienne 
des  environs  de  Hof,  en  Bavidre. 
Prague  et  Paris,  1868. 

Olenus,  Conocephalites,  Arethusina,  Caly- 
mene, Bavarilla  n.  g.,  Lichas , Asaphus,  Cheiru- 
rus, Agnostus. 

Trilobites.  I.  Rdsumd  gdndral  de 

nos  dtudes  sur  Involution  des  Trilo- 
bites. II.  Distribution  verticale  des 
Trilobites  dans  le  bassin  silurien  de  la 
Boheme.  III.  Paralldle  entre  les  Tri- 
lobites et  Cdphalopodes  siluriens  de  la 
Boheme.  IV.  Flpreuve  des  tlidories  pa- 
ldontologiquos  par  la  rdalitd.  Prague 
et  Paris,  1871. 

Systdme  silurien  du  centre  de  la 

Bobdme.  lre  partie.  Recherches  pa- 
ldontologiques.  Supplement  au  vol.  1. 


16 


A BIBLIOGRAPHY  OF  PALEOZOIC  CRUSTACEA. 


' iBULL.  63. 


Barrande  (Joachim)— Continued. 
Trilobites.  Crustac^s di vers  et poissons. 
Prague  et  Paris,  1^72,  32  pis. 

Trilobites.  Harpes,  Remopleurides , Paradoxi- 
des,  Plutonia,  Anopolenus,  Dikelocephalus,  Doli- 
chometopus,  Hydrocephalus , Olenus,  Olenellus, 
Bohemilla , Conocephalites,  Aneuacanthus,  An- 
gelina, Anomocare,  Arionellus,  Atops,  Bathyu- 
rus,  Ghariocephalus,  Corynexochus,  Ellipsoce- 
phalus,  Holocephalina,  Ptychaspis,  Sao,  Triar- 
thrus,  Triarthrella,  Proetus,  Arethurina,  Gar- 
mon n.  g.,  Cyphaspis,  Cyphoniscus,  Harpides, 
Isocolus , Phillipsia . Phacops,  Dalmanites,  Caly- 
mene,  Pavarilla,  Homalonotus,  Lichas,  Trinu- 
cleus, (Lmpyx,  Dionide,  Endymionia,  Microdis- 
cus, Asaphus,  Barrandia,  Ogygia,  Psiloceplialus, 
Stygina,  JEglina,  Illcenurus,  Acidaspis,  Cheiru- 
rus,  Areia,  Crotalurus,  Deiphon,  Placoparia, 
Sphcerexochus,  Staurocephalus,  Zethus,  Dindy- 
mene,  Amphion,Cromus,  Encrinurus,  Bronteus, 
lllcenus,  Nileus,  Agnostus,  lllcenopsis,  Pemphi- 
gaspis,  Shumardia , Telephus  n.  g.,  Tnopus. 

Phyllopoda.  Geratiocaris,  Aptychopsis  n.  g., 
Cryptocaris n gM  Pterocaris  n.  g. 

Ostracodes.  Aristozoe  u.  g.,  Beyrichia,  Bol- 
bozoe  n.  g.,  Callizoe  n.  g.,  Caryon  n.  g.,  Grescen- 
tilla  a.  g.,  Cythere , Cytheropsis  n.  g.,  Elpc  n.  g , 
Entomis,  Hippa  n.  g.,  Isochilina,  Leperditia, 
Nothszoe  u.  g.,  Orozoe  n.  g.,  Primitia,  Zonozoe 
n.  g. 

Eurypteridae.  Pterygotus,  Eurypterus. 

Cirrhipedise.  Anatifopsis  n.  g.,  Plumulites  n. 
g.,  Bactropus  n.  g , Dryalus  n.  g. 

See  Oorda  (A.  J.  C.)  and  Hawle  (Ignaz),* 

and  Verneuil  (E.  de).  See  Verneuil 

(E.  de)  and  Barrande  (Joachim). 

Barrett  (S.  T.)  The  coralline  or  Niagara 
limestone  of  the  Appalachian  system  as 
represented  at  Nearpass’s  Cliff,  Mon- 
tague, N.  J. 

In  A®.  Jour.  Sci.,  3d  series,  vol.  15, 1878,  p. 
370. 

Proetus  pachydermatus  n.  s. 

Description  of  a new  Trilobite,  Dal- 
manites dentata. 

In  Am.  Jour.  Sci.,  3d  series,  vol.  11,  1876,  p. 
200,  plate. 

On  Dalmanites  dentata. 

In  Am.  Jour.  Sci.,  3d  series,  vol.  12, 1876,  p.  70. 

Barris  (W.  H.)  New  fossils  from  the 
Corniferous  formation  at  Davenport. 

In  Davenport  Acad.  Nat.  Sci.,  vol.  2,  1879,  p. 
282,  pis.  10  and  11. 

Proetus  davenportensis  n.  s.,  pi.  11,  fig.  8. 

Barrois  (Charles).  Note  sur  des  fossiles 
de  Catheryielle. 

In  Bull.  Soc.  G6ol.  France,  3d  series,  vol.  8, 

1880,  p.  266. 

Phacops  fecundus,  Dalmanites  hausmani, 

pi.  8. 


Barrois  (Charles) — Continued. 

Recherches  sur  les  terrains  anciens 

des  Asturies  et  de  la  Galice. 

In  M6m.  Soc.  G6ol.  Nord,  Lille,  vol.  2,  1882, 
(*30  pp.,  20  pis. 

Paradoxides,  Conocephalus,  Arionellus. 

Sur  les  faunes  siluriennes  de  la 

Haute-Garonne.  Pis.  6,  7. 

In  Annales  Soc.  G6ol.  Nord,  Lille,  vol.  10, 
1883,  p.  151. 

Cyphaspis,  Phacops,  Dalmanites,  Lichas. 

Les  appendices  des  Trilobites. 

In  Annales  Soc.  G6ol.  Nord,  Lille,  vol.  11, 
1883-  84,  p.  228. 

Memoire  sur  le  calcaire  & Polypiers 

de  Cabri&res  (H6rault). 

In  Annales  Soc.  G6ol.  Nord,  Lille,  vol.  13, 
1885-’86,  p.  74,  plate. 

Phacops,  Bronteus. 

Sur  la  faunede  Haut-de-Ver  (Haute- 

Garonne). 

In  Annales  Soc.  G6ol.  Nord,  Lille,  vol.  13, 
1885- ’86,  pis.  2,3. 

Harpes,  Cyphaspis,  Phacops,  Dalmanites, 
Lichas , Bronteus. 

Sur  le  calcaire  ddvonien  de  Chaude- 

fonds  (Maine-et-Loire). 

In  Annales  Soc.  G6ol.  Nord,  Lille,  vol.  13, 
1885-’86,  p.  170. 

Aper^u  de  la  constitution  g^ologique 

de  la  rade  de  Brest. 

In  Bull.  Soc.  G6ol.  France,  3d  series,  vol.  14, 
1886,  p.  678,  pis.  31-33. 

Homalonotus  le  Hiri  Barrois. 

Baumer  (J.  W.)  Naturgeschichte  des 
Mineralreichs  mit  besonderer  Anwen- 
dung  auf  Thiiringen.  2 vols.  Gotha, 
1763-64,  1767. 

Bayle  (E.)  Explication  de  la  carte  gdo- 
logique  de  la  France.  Yol.  4.  Atlas. 
Paris,  1878. 

Premiere  partie.  Fossiles  principaux  des 
terrains. 

PI.  1,  Megalaspis ; pi.  2,  Homalonotus,-  pi.  3, 
Galymene  pi.  4,  Gheirurus , lllcenus,  Phacops, 
Cryphceus,  Goldius,  Proetus,  Phillipsia;  pi.  5, 
Acidaspis. 

Bean  (W.)  Entomostracans  from  the 
Coal  Measures  of  Newcastle-upou-Tyne. 

In  Mag.  Nat.  Hist.  (London),  vol.  9,  1836,  p. 
376. 

Beyrichia. 

Beckmann  (J.)  Commentatio  de  reduc- 
tione  rerum  fossilium  ad  genera  natu- 
ralia  protyporum. 

In  Novi  Comm.  Soc.  Scient.  Gotting.,  vol.  3, 
1773,  p.  95. 


•‘'OGDEB.J 


LIST  OF  AUTHORS. 


17 


Beecher  (C.  E.)  Ceratiocaridce  from  the 
Upper  Devonian  Measures  in  Warren 
County. 

In  Second  Geol.  Survey  Pennsylvania,  vol. 
PPP,  1884,  2 pis. 

Echinocaris,  Elymocaris  n.  g.,  Tropidocaris 
n.  g. 

Author’ s edition  issued  separately,  entitled: 
“ Ceratiocaridce  from  theChemung  and  Waverly 
Groups  at  "Warren,  Pa.,”  with  2 pis.,  Harris- 
burg, 1884,  22  pp. 

Belt  (Thomas).  On  some  new  Trilobites 
from  the  Upper  Cambrian  rocks  of  North 
Wales. 

In  Geol.  Mag.,  vol.  4,  London,  1867,  p.  294,  pi. 

12. 

Agnostus  pisiformis,  A.  nodosus,  Olenus  gib- 
bosus. 

On  the  Lingula  flags  or  Festiniog 

group  of  the  Dolgelly  district. 

In  Geol.  Mag.,  vol  5,  London,  1868,  p.  5,  pi.  2. 

Conocoryphe,  Sphcerophthalmus , Agnostus. 

Bergeron  (M.-T.)  Etude  paldontologi- 
que  et  stratigraphique  des  terrains 
anciens  de  la  montagne  Noire. 

In  Bull.  Soc.  G6ol.  France,  3d  series,  vol.  15, 
1887,  No.  5. 

Harpes,  Phacops,  Cheirurus. 

Beushausen  ( Louis ).  Beitrage  zur 
Kenntniss  des  oberharzer  Spiriferen- 
sandsteins  und  seiner  Fauna.  (*) 

Inaugural-Dissertation.  Gottingen,  1884,  p. 
34. 

Beyrich  (Ernst).  Ueber  einige  bohmi- 
sche  Trilobiten.  Berlin,  1845,  1 pi. 

Lichas,  Cheirurus  n.  g.,  Sphcerexochus  n.  g., 
Bronteus , Battus,  Trochurus  n.  g. 

Untersuchungen  iiber  Trilobiten. 

Zweites  Stuck  als  Fortsetzung  zu  der 
Abhandlung  “Ueber  einige  bohmische 
Trilobiten.”  Berlin,  1846,  3 pis. 

Harpes.  Harpid.es  n.  g.,  Proetxis,  Calymene, 
Lichas.  Trinucleus.  Odontopleura,  Cheirurus , 
Sphcerexochus.  Arges,  Bronteus. 

Bigsby  (J.  J.)  Description  of  a new 
species  of  Trilobite. 

In  Jour.  Acad.  Nat.  Sc.  Phila.,  vol.  4,  pt.  2, 
1825,  p.  365,  pi.  23. 

Paradoxides  boltoni  ( Lichas  boltoni). 

■  Thesaurus  Siluricus.  The  flora  and 

fauna  of  the  Silurian  period.  London, 

1868. 

Billings  (E  ) Fossil  foot  prints. 

In  Canadian  Naturalist,  vol.  1,  1856,  p.  35, 
wood-cuts. 

Protichnites  septem  notatus. 

■  On  some  of  the  characteristic  fossils 

of  the  Lower  Silurian  rocks  of  Canada. 

Bull.  63 2 


Billings  (E.)— Continued. 

In  Canadian  Naturalist,  vol.  1,  1856,  p.  39,  11 
wood- cuts. 

The  author  figures  Isotelus  gigas , Calymene 
senaria,  and  the  hypostoma  of  Isotelus  gigas. 

— — Fossils  of  the  Upper  Silurian  rocks, 
Niagara  and  Clinton  groups. 

In  Canadian  Naturalist,  vol.  1, 1856,  p.  57, 1 pi. 

Phacops  limulurus  Green. 

Description  of  fossils  occurring  in 

the  Silurian  rocks  of  Canada. 

In  Canadian  Naturalist,  vol.  1, 1856,  p.  312, 10 
wood-cuts. 

Homalonotus  delphinocephalus  Green. 

Report  for  the  year  1856  of  E.  Bil- 
lings, esq.,  palaeontologist,  addressed 
to  Sir  Wm.  E.  Logan,  etc. 

In  Geol.  Survey  Canada.  Kept,  Progress,  1853- 
’54-’55-’56,  p.  247. 

Triarthrus  spinosus  n.  s.,  Acidaspis  horani 
n.  s.,  Bronteus  lunatus  n.  s. 

Fossils  of  the  Calciferous  saudrock, 

including  those  of  a deposit  of  white 
limestone  at  Mingau,  supposed  to  be- 
long to  the  formation. 

In  Canadian  Naturalist,  vol.  4, 1859,  p.  345, 12 
wood  cuts. 

Bathyurus  n.  g.,  Leperditia. 

Description  of  some  new  species  of 

Trilobites  from  the  Lower  and  Middle 
Silurian  rocks  of  Canada. 

In  Canadian  Naturalist,  vol.  4, 1859,  p.  367, 18 
wood-cuts. 

Triarthrus,  Amphion,  lllcenus. 

Fossils  of  the  Chazy  limestone,  with 

descriptions  of  new  species. 

In  Canadian  Naturalist,  vol.  4, 1859,  p.  426,  38 
wood-cuts. 

Harpes,  Bathyurus,  Leperditia. 

Description  of  some  new  species  of 

fossils  from  the  Lower  and  Middle  Silu- 
rian rocks  of  Canada. 

In  Canadian  Naturalist,  vol.  5,  1860,  p.  49,  16 
wood-cuts. 

Proetus,  Phacops,  Dalrnanites,  Cheirurus. 

On  some  new  species  of  fossils  from 

the  limestone  near  Point  Levi,  opposite 
Quebec. 

In  Canadian  Naturalist,  vol.  5,  I860,  p.  301,  30 
figs. 

Dikelocephalus , Conocephalites,  Arionclhis, 
Bathyurus , Menocephalus,  Asaphus,  Cheirurus, 
Agnostus. 

On  some  of  the  rocks  and  fossils 

occurring  near  Phillipsburg,  Canada 
East. 

In  Canadian  Naturalist,  vol,  6,  1861,  p.  310,  6 
figs. 

Bathyurus,  Menocephalus,  Amphion. 


18 


[bull.  63. 


A BIBLIOGRAPHY  OF  PALEOZOIC  CRUSTACEA. 


Billings  (E.) — Continued. 

On  some  new  or  little-known  species 

of  Lower  Silurian  fossils  from  the  Pots- 
dam group  (Primordial  zone).  Mon- 
treal, 1861,  24  pp. 

Tliis  pamphlet,  with  the  addition  of  a de- 
scription of  Archceocyathus  profundus,  the  sup- 
pression of  that  of  A.  minganensis,  and  the 
notes  on  pages  10,  11,  and  12,  was  reprinted  in 
the  “Palaeozoic  Fossils  of  Canada,”  vol.  1, 
1865,  pp.  1-24,  also  in  part  in  the  “Geol.  Ver- 
mont,” vol.  2, 1861,  pp.  942-960. 

Olenellus  thompsoni  Hall,  Olenellus  vermon- 
tana  Hall,  Oonocephalites  miser  n.  s.,  C.  adamsi 
n.  -s.,  0.  teucer,  O.  vulcanus  n.  s.,  C.  arenosus  n. 
s.,  Bathyurus  senectus  n.  s.,  B.  parvulus  n.  s., 
Ampyx  halli  n.  s. 

Description  of  a new  species  of 

Harpes  from  the  Trenton  limestone, 
Ottawa. 

In  Canadian  Naturalist,  vol.  8,  1863,  p.  36, 
wood-cut. 

Harpes  dentoni  n.  s. 

Geological  Survey  of  Canada.  Re- 
port of  progress  from  its  commence- 
ment to  1863.  Illustrated  by  498  wood 
cuts  in  the  text.  Montreal,  1863.  Atlas 
of  maps  and  sections. 

Harpes,  Paradoxides,  Conocephalites,  Triar- 
thrus,  Bathyurus,  Proetus,  Phaeops,  Dalma- 
nites,  Calymene,  Lichas,  Trinucleus , Asaphus, 
Illamus,  Acidaspis , Gheirurus,  Amphion , En- 
crinurus, Bronteus,  Beyrichia,  Leperditia, 
Isochilina,  Eurypterus,  Gytheropsis. 

— Description  of  new  species  of  Phil- 
lipsia  from  the  Lower  Carboniferous 
rocks  of  Nova  Scotia. 

In  Canadian  Naturalist,  vol.  8,  1863,  p.  209,  1 
wood-cut. 

Phillipsia  howi. 

Description  of  some  new  species  of 

fossils,  with  remarks  on  others  already 
known,  from  the  Silurian  and  Devonian 
rocks  of  Maine. 

In  Proc.  Portland  Soc.Nat.  Hist.,  vol.  1, 1869, 
p.  104,  plate. 

Dalmanites  epicrates  n.  s.,  Gheirurus  tarqui- 
nius  n.  s.,  Proetus  junius  n.  s.,  P.  macrobius 
n.  s.,  Bronteus  pompilius  n.  s.,  Phaeops  trajanus 
n.  s.,  Lichas. 

Palseozoic  fossils.  Yol.  1.  Contain- 
ing descriptions  and  figures  of  new  or 
little  known  species  of  organic  remains 
from  the  Silurian  rocks.  1861-’65.  426 
pp.,  401  figures.  Geol.  Survey  Canada,  i 

The  first  portion  of  this  work,  consisting  of 
24  pages,  was  issued  in  November.  1861,  and  I 
re-appears  in  this  work,  with  the  exception  cf  [ 
the  notes  on  pages  10,  11,  and  12  of  the  original 
edition.  The  second  part,  consisting  of  pp.  ! 


Billings  (E.) — Continued. 

25-56,  was  issued  in  January,  1862,  and  the 
third,  pp.  57-168,  in  June,  1862;  the  fourth, 
pp.  169-344,  in  February,  1865. 

Harpes,  Remopleurides,  Olenus,  Olenellus , 
Dolichometopus,  Dikelocephalus,  Telephus , Cono- 
cephdlites,  Ari&nellus,  Bathyurus,  Loganellus , 
Henocephalus,  Triarthrus,  Harpides,  Lichas, 
Ampyx,  Asaphus,  Gheirurus , Sphcerexochus, 
Amphion,  Encrinurus,  Illcenus,  Nileus,  Agnos- 
tus,  Beyrichia,  Leperditia,  Bathyurellus  n.  g., 
Shumardia  n.  g..  Endymion  n.  g.  (this  name 
was  changed  by  the  author  tp  that  of  Endy- 
mionia  on  p.  281). 

Catalogue  of  the  Silurian  fossils  of 

the  island  of  Anticosti,  with  descrip- 
tions of  some  new  genera  and  species. 
1866.  93  pp.,  28  figs.  Geol.  Survey 

Canada. 

Harpes,  Sphcerocoryphe,  Proetus,  Dalmani- 
tes, Calymene,  Lichas,  Dionide,  Asaphus,  Chei- 
rurus , Sphcerexochus,  Encrinurus,  Bronteus, 
Illcenus,  Beyrichia,  Leperditia. 

Note  on  some  specimens  of  Lower 

Silurian  Trilobites. 

In  Quart.  Jour.  Geol.  Soc.  London,  vol.  26, 
1870,  p.  479,  pis.  31,  32. 

Asaphus  platycephalus  Stokes,  with  some  of 
the  legs  preserved. 

Palaeozoic  fossils.  Yol.  2,  pt.  1. 

1874. 

In  Geol.  Survey  Canada,  144  pp.,  35  figs,  and 
9 pis. 

Paradoxides,  Anopolenus,  Agraulos,  Soleno 
pleura. 

On  some  new  or  little  known  fossils 

from  the  Silurian  and  Devonian  rocks 
of  Canada. 

In  Canadian  Naturalist,  new  series,  vol.  7, 
1874,  p.  230. 

Lichas  superbus  n.  s. 

Blumenbach  (J.  F.)  Abbildungen  na- 
turhistorischer  Gegenstande.  Gottin- 
gen, 1810. 

The  author  remarks  on  a species  of  Calymene 
blumenbachii,  which  he  figures  on  pi.  50,  that 
“according  to  all  analogy  it  must  have  been 
without  doubt  the  petrifaction  of  some  species 
of  insect  without  wings.” 

The  specimen  was  from  Dudley  limestone 
and  afterwards  named  by  Alex.  Bronguiart 
Calymene  blumenbachii. 

Boeck  (C.)  Notitzer  til  Laeren  om  Tri- 
lobiten.  . (*) 

In  Nyt  Mag.  Naturvid.,  vol.  1,  Christiania, 
1827,  p.  11. 

Trilobitem  tesseni,  T.  spinosus  major,  T. 
spinosus  minor,  T.  gracilis,  T.  zippei,  T.  haus - 
manni. 

Noticed  in  Bull.  Sci.  Nat.  (Ferussac),  vol. 
14,  1828,  p.  45. 


VOGDES.] 


LIST  OF  AUTHORS. 


19 


Boeck  (C.) — Continued. 

Uebersicht  der  bisber  in  Norwegen 

gefundenen  Formen  der  Trilobiten- Fa 
milie.  (*) 

In  Gaea  Norwegica  (Keilliau),  Christiania, 
1838,  pt.  1,  p.  138. 

Trilobiten  elliptifrons , T.  elegans , T.  haus- 
manni . T.  semilunaris , T.  punctatus,  T.  sphce- 
ricus,  T.  clavifrons,  T.  blumenbachii , T.  fischeri, 
T. forficula,  T.  acicularis,  T.  lyra , T.  grandis,  T. 
angustifrons,  T.  dilatatus,  T.  expansus,  T.  acu- 
munatus,  T.  limbatus , T.  striatus,  T.  f rontalis , 
T.  crassicauda,  T.  centrotus,  T.  asellus,  T.  alatus, 
T.  latus,  T.  granulatus,  T.  rostratus,  T.  mammil- 
latus , T.  scaraboeoides. 

Om  Trilobiten. 

In  Skand.  Naturf.  Forhand.,  vol.  2,  1840,  p. 
289;  Neues  Jahrbuck  fur  Mineral.,  1841,  p.  724. 

Boll  (Ernst).  Beitrag  zur  Kenntniss  der 
Trilobiten. 

In  Danker  and  von  Meyer’s  P alaeon togra p h - 
ica,  vol.  1,  Cassell,  1847,  p.  126. 

A inpyx,  Battus. 

Ueber  die  Arten  der  Gattung  Bey- 

richia  in  norddeutschen  Silurian-Gerol- 
len. 

In  Zeitschr.  deutsch.  geol.  Gesell.,  Berlin, 
vol.  8,  1856,  p.  321, 4 figs. 

A communication  from  Herr  Boll  to  Herr 
Bey  rich. 

Beyrichia  jonesi,  B.  spinulosa,  B.  1 nans. 

Die  Beyricliien  der  norddeutschen 

silurischen  Gerdlle. 

In  Afchiv  Yereins  FreundeNaturg.  Mecklen- 
burg, 1862,  p.  114,  pi.  1. 

Beyrichia. 

Born  ( Chev . de).  Lithophilacion  Bor- 
nianum.  Index  fossilium  quae  colleget 
in  class,  ac  ordinis  digessit.  2 vols. 
Pragac,  1772.  (*) 

In  Crustacea,  vol.  2,  p.  5. 

Bornemann  (J.  G.)  Palaeontologisckes 
aus  dem  cambrischen  Gebiete  von  Ca- 
malgrande  in  Sardinien. 

In  Zeitschr.  deutsch.  geol.  Gesell.,  Berlin, 
1883,  p.  270. 

Olenellus  zoppei,  Conocoryphe  sp.?  (Olenus 
armatu8  Meng.),  lllcenus  meneghini. 

Bradley  (Frank).  Description  of  a new 
Trilobite  from  the  Potsdam  sandstone, 
with  a note  by  E.  Billings,  of  Montreal, 
CaDada. 

In  Proc.  Am.  Assoc.  Adv.  Sci.,  14th  meeting 
1861,  p.  161,  3 wood-cuts. 

• Oonocephalit.es  minutus. 

See,  also,  Am.  Jour.  Sci.,  2d  series,  vol.  30, 
1860.  p.  241;  Canadian  Naturalist,  vol.  5,  1860, 
p.  420. 


Brady  (M.  P.)  See  Jones  (T.  Rupert), 
Kirkby  (J.  W.)  and  Brady  (M.  P.). 

Brocchi  (M.  P. ) Note  sur  un  crustacd 
fossile  recueilli  dans  les  schistes  d’Au- 
tun. 

In  Bull.  Soc.  G6ol.  France,  3d  series,  vol.  8, 
No.  1,  1880,  p.  3,  pi.  1. 

Paloeocaris,  Gampsonyx,  Nectotelson  n.  g. 

Brodie  (P.  B.)  History  of  fossil  insects 
in  the  Secondary  rocks  of  England. 
London,  1845,  pp.  105-115,  pi.  1,  fig.  11. 

This  author  describes  and  figures  a fossil 
from  Coalbrookdale  resembling  the  caterpillar 
of  the  Emperor  moth,  which  was  afterwards 
described  by  J.  W.  Salter  under  the  name  of 
Eurypterus  {Arthropleura)  ferox. 

Brogger  (W.  C.)  Fossiler  fra  Oxna  og 
Kletten.  (*) 

In  Geol.  Foreningens  Stockholm  Fbrhandl., 
vol.  2,  1875,  1 pi. 

Paradoxides,  Liostracus,  Agnostu ®. 

Andrumkalk  ved  Breidengen  val- 

ders. 

In  Geol.  Foreningens  Stockholm  Forhandl., 
vol.  3,  1876,  1 pi. 

Paradoxides,  Liostracus,  Selenopleura,  Ag- 
nostus. 

Om  Trondhjemsfeldtets  midlere 

Afdeling  mellem  Guldalen  og  Meldalen 
Christiania.  (*) 

In  Vidensk.  Selskab.  Forhandl.,  1877,  No.  2, 
p.  1,  2 pis. 

Dalmanites , Trinucleus. 

Om  Paradoxides  skifrene  ved.Krek- 

ling.  (*) 

In  Nyt  Mag.  Naturvid.,  vol.  24,  pt.  1,  1878, 
6 pis. 

Paradoxides,  Olenellus,  Dolichometopus,  Lio- 
stracus, Conocoryphe,  Inomocare,  Elyx,  Soleno- 
pleura,  Ellipsocephalus,  Arionellus,  Agnostus. 

Die  silurischen  Etagen  2 und  3 im 

Kristianiagebiet  und  auf  Eker.  Kristi- 
ania,  1882,  12  pis. 

Remopleurides,  Dicelocephalus,  Olenus,  Para- 
bolina,  Peltura,  Cyclognathus,  Ceratopyge, 
Ctenopyge,  Protopleura  (new  subgenus  to  the 
genus  Peltura ),  Parabolinella  (new  subgenus 
to  the  g'mus  Olenus),  Leptoplastus,  Sphceroph - 
tlialmus,  Eurycare,  Bceckia  n.  g.,  Triarthrus, 
Euloma,  Holometopus,  Harpides,  Phacops, 
Lichas,  Trinucleus,  Ampyx,  Asaphus,  Mega- 
laspis,  Symphysurus,  Niobe,  Ptychopyge,  Nileus, 
Oheirurus,  lllcenus,  Dysplanus,  Amphion, 
Gybele,  Agnostus,  Oonophrys,  Beyrichia,  Leper - 
ditia,  l8ochilina. 

Paradoxides  olandicus  nivaet  ved 

Ringsaker,  Norge.  (*) 

In  Geol.  Foreningens  Stockholm.  Forhandl, 
vol.  6,  1884,  1 pi. 


20 


A BIBLIOGRAPHY  OF  PALEOZOIC  CRUSTACEA. 


[BULL.  63. 


Brogger  (W.  C.) — Continued. 

Om  aldern  af  Olenelluszonen  i Nord- 

amerika. 

In  Geol.  Foreningens  Stockholm  Forhandl., 
vol.  8, 1886,  p.  182. 

TJeber  die  Ausbildung  des  Hyposto- 

mes  bei  einigen  skandinavischen  Asa- 
pbiden. 

In  Ofversigt  Kongl.  Svenska  Yet. -Acad. 
Handl.,  vol.  11,  1886,  3 pis. 

Asaphus,  Isotelus,  Ptychopyge,  Megalaspis, 
Megalaspides  n.  g.,  Niobe,  Asaphellus,  Ogygia, 
Nileus,  Symphysurus. 

Bromell  (M.)  Lithographia  Suecana. 

In  Acta  Literaria  Suecise,  vol.  2,  TJpsalise, 
1725,  p.  63. 

This  work  was  continued  in  several  parts 
through  this  volume,  hut  it  is  only  at  p.  493, 
in  the  section  called  “De  lapidibus  insectiferis 
Scanices  et  Gothicis,”  that  the  Trilobites  are 
treated.  We  have  there  the  Oleni  of  the  alum 
slate  and  Agnostus  pisiformis. 

A separate  edition  of  the  work  was  printed 
at  Stockholm  and  Leipzig,  in  1740,  hearing  the 
same  title  as  the  original  work. 

Brongniart  (Alex.)  Histoire  naturelle 
des  Crnstiac^s  fossiles  sous  les  rapports 
zoologique  et  g^ologique,  savoir  les 
Trilobites.  Les  Crustac^s  proprement 
dits  par  A.-G.  Desmarest.  11  pis. 
Paris,  1822. 

This  author  was  the  first  systematic  writer 
upon  the  Trilobites.  He  arranges  twenty-two 
species  under  five  new  generic  names,  as  fol- 
lows : First  genus,  Galymene,  species  1.  G.  de 
Blumenbach,  2.  C.  de  Tristan,  3.  G.  ? variolaire, 
4.  G.  ? macrophtalme.  Second  genus,  Asaphus, 
species  1.  A.?  cornigere,  2.  A.  de  Debuch,  4. 
A.  caudigere,  5.  A.  large  queue.  Third  genus, 
Ogygia,  species  1.  O.  de  Guettard,  2.  O.  de 
Desmarest.  Fourth  genus,  Paradoxides,  spe- 
cies l.P.de  Tessin,  2.  P.  spinuleux,  3.  P.  scar  a- 
bo'ide,  4.  P.  ? gibbeux,  5.  P.  lacinie.  Esp&ces  de 
genre  incertain : Trilobite  granule,  T.  ponctue, 
T.  bucephale,  T.  tentacule.  Fifth  genus,  Ag- 
nostus, species  1.  A.  pisiforme. 

- and  Desmarest  (A.-G.)  Histoire 

naturelle  des  Trilobites  et  des  Crustac^s 
fossiles. 

In  Jour.  Mines,  vol.  9,  1822,  p.  273. 

Bronn  (Heinrich).  Ueber  zwei  neue  Tri- 
lobiten-Arten. 

In  Zeitschr.  fur  Mineral.,  vol.  1,  pt.  1, 1825,  p. 
317,  pi.  2. 

Galymene  latifrons,  G.  schlotheimi. 

Geognostische  zoologische  Unter- 

suchungen  in  den  russisch-baltischen 
Provinzen  von  Herrn  Dr.  Eduard  Eich- 
wald. 

In  Zeitschr.  fur  Mineral.,  vol.  for  1828,  pt.  1, 
p.  104. 


Bronn  (H.  G.)  Lethsea  geognostica,  oder 
Abbildungen  and  Beschreibungen  der 
fur  die  Gebirgs-Formationen  bezeich- 
nendsten  Yersteinerungen.  Stuttgart, 
1835-’38. 

2 vols.,  and  atlas  with  47  pis. 

and  Roemer  (F.)  H.  G.  Bronn’s 

Lethaea  geognostica,  oder  Abbildungen 
und  Beschreibungen  der  fur  die  Gebirgs- 
Formationen  bezeichnendsten  Yerstei- 
nerungen. 3d  ed.  Stuttgart,  1851-’56. 

3 vols.  and  atlas,  124  pis. ; vol.  1,  p.  525. 

Harpes,  Harpides,  Remopleurides,  Paradoxi- 
des, Hydrocephalus f Sao,  Arionellus,  Ellipso- 
cephalus,  Olenus , Gonocephalites,  Proetus,  Gy- 
phaspis,  Phillipsia,  Arethusina,  Phacops,  Dal- 
mania,  Cryphceus,  Galymene , Homalonotus, 
Lichas,  Trinucleus,  Ampyx,  Dionide,  Asaphus, 
Ogygia,  JEglina,  lllcenvs,  Addas  pis,  Ceraurus, 
Placoparia,  Splicer exochus,  Staurocephalus,  Dei- 
phon,  Dindymene,  Zetheis,  Amphion,  Enerinu- 
rus,  Cromus,  Bronteus,  Telephus,  Agnostus,  Eu- 
rypterus,  Himantopterus,  Pterygotus,  Limulus, 
Gampsonychus , Cythere,  Bairdia,  Cypridina, 
Cyprella,  Entomoconchus,  Beyrichia,  Dithyro- 
caris,  Ceratiocaris. 

Note  iiber  die  mit  Homalonotus  ver- 

wandten  Trilobitengenera. 

In  Neues  Jahrbuch  fur  Mineral.,  1840,  p.  445, 
pi.  8,  figs.  1 a,  o. 

Index  palseontologicus,  oder  Ueber- 

sicht  der  bis  jetzt  bekannten  fossilen 
Organismen,  unter  Mitwirkung  der 
HH.  H.  R.  Goppert  und  Herm.  von 
Meyer  bearbeitet  von  Dr.  H.  G.  Bronn, 
Nomenclator  palseontologicus  in  alpha- 
betischer  Ordnung.  Stuttgart,  1848, 
3 vols. 

Ueber  Gampsonyx  Jimbricatus  Jordon 

aus  der  Steinkohlen  - Formation  von 
Saarbriicken  und  vom  Murg-Thal. 

In  Neues  Jahrbuch  fur  Mineral.,  1850,  p.  575. 

Briickmann  (F.  E.)  Epistolarum  itine- 
rariarum  centuria.  Wolfenbiittelse,  3 
vols. 

In  Epist.  23,  pi.  2,  figs.  1-7, 1732,  and  Epist.  64, 
pi.  3,  fig.  5, 1737. 

This  author  compares  the  fossil  Crustacea 
with  the  Mollusca  and  calls  them  Armata 
veneris. 

Brunnich  (M.  T. ) Beskrivelse  over  Trilo- 
biten,en  Dyrestagt  og  dens  Arter,  med 
en  ny  Aftegning. 

In  Nye  Samling  of  detKongelige  Danske  Yi, 
denskabers  Selskabs  Skriften,  Kiobenhavn- 
1781,  p.  384. 1 pi. 

This  author  describes  Trilobus  ( Galymene ) 
tuberculatus,  Trilobus  \Dalmanites)  caudatus 
(figures  of  head  and  pygidiura),  Trilolus  dilctr 
tatus,  Trilobus  ( Encrinurus ) punctatus. 


WJGDES.] 


LIST  OF  AUTHORS. 


21 


Such  (Leopolu  von).  Beitrage  zur  Be- 
stimmung  der  Gebirgs-Formationen  in 
Russian  d. 

In  Archiv  mineral.  Geogn.,  etc.,  vol.  15,  Ber- 
lin, 1841,  p.  1,  pi.  2. 

Phacops,  Oalymene,  Asaphus,  Illcenus. 

Buckland  ( William ).  Geology  and 
mineralogy  considered  with  reference 
to  natural  theology.  Bridgewater  trea- 
tise. 2 vols.  London,  1837,  87  pis. 
[4th  ed.,  London,  1869,  2 vols.,  90  pis.] 

Translated  into  German  by  L.  A gassiz. 

Paradoxides , Phillipsia,  Phacops,  Calymene, 
Asaphus,  Ogygia,  Encrinurus,  Limulus  (Beli- 
nuru8)  trilobitoides. 

Burmeister  (H  ) Die  Organisation  der 
Trilob iten,  etc.  Berlin,  1843,  6 pis. 

The  English  translation  is  entitled:  “The 
organization  of  Trilobites  deduced  from  their 
living  affinities,  with  a systematic  review  of  the 
species  hitherto  described,  by  Hermann  Bur- 
meister, edited  from  the  German  by  Prof* 
Thomas  Bell,  E.  R.  S.,  and  Prof.  E.  F.  Forbes, 
F.  R.  S.”  London,  Ray  Society,  1846  There  is 
a supplementary  appendix  by  the  editors. 

Burmeister  classifies  63  species  under  23 
genera  arranged  in  the  following  order  : 

Eurypterus,  Cytkerina,  Trinucleus , Ogygia , 
Odontopleura,  Arges,  Bronteus , Paradoxides , 
Olenus , Conocephalus,  Ellipsocephalus.  Earpes , 
Calymene,  Homalonotus,  Phacops,  Cyphaspis 
n.  g.,  Proetus,  ASonia  n.  g.,  Archegonus  n.  g., 
Illcenus,  Dysplanus  n.  gM  Asaphus,  Ampyx. 

The  supplementary  appendix  by  Thomas 
Bell  and  E.  F.  Forbes  contains  an  alphabetical 
list  of  British  Trilobites,  also  a copy  of  McCoy’s 
generic  description  of  the  following  genera: 
Tiresia,  Forbesia,  Portlockia,  Trinodus  (Synop- 
sis Silurian  Fossils  Ireland,  1846) ; the  generic 
descriptions  of  Cheirurus , Sphcerexochus , 
Eichas,  Trochurus  (Beyrich,  Ueber  einige  boh- 
mische  Trilobiten,  1845),  and  a list  of  the  genera 
and  species  described  by  Barrande  (Notice  pr6- 
liminaire  sur  le  syst^me  silurien  et  les  Trilo- 
bites de  Boh6me,  1846). 

and  Alton  (Ed.  de).  Neue  Beo- 

bachtungen  Uber  die  Organisation  der 
Trilobiten.  (*) 

In  Zeitungfur  Zoologie,  Zootomie  und  Palaio- 
zoologie,  Alton  und  Burmeister,  Leipzig,  vol. 
1, 1848,  p.  67,  pi.  1,  figs.  13-19. 

Callaway  (Charles).  On  a new  area  of 
Upper  Cambrian  rocks  in  South  Shrop- 
shire, with  a description  of  a new  fauna. 

In  Quart.  Jour.  GeoL  Soc.  London,  vol.  33, 
1877,  p.  652,  plate. 

Olenus,  Gonocoryphe,  Asaphus,  Asaphellus 
(new  subgenus),  Platypeltes  (new  subgeuus), 
Lichapyge  n.  g.,  Agnostus,  Conophrys  n.  g. 

Castelnau  (Laport  de).  Communique  h 
PAcaddmie  des  sciences  de  Paris  la  d6- 


Castelnau  (Laport  de) — Continued, 
couverte  des  pieds  des  Trilobites  qu’il 
aurait  vus  dans  l’int6rieur  d’un  exeui- 
plaire  enroul6  de  PAmfhique  du  Nord. 

In  Inst.  France,  1842,  p.  74 ; Neues  Jahrbuch 
fur  Mineral.,  1843,  p.  504;  Comptes  Rendus, 
vol.  14,  1842,  p.  344. 

Calymene. 

Essai  sur  le  syst&me  silurien  de 

PAmdrique  Septentrionale.  Paris,  1843, 
27  pis. 

Asaphus  micrurus,  A.  limulurus,  A.  cordieri, 
A.  caudatus,  A.  edwardii,  A.  murchisoni,  Ho- 
malonotus  giganteus,  II.  herculaneus,  H.  atlas, 
Arctinurus  n.  g.,  A.  boltoni,  Calymene  bufo, 
Odontocephalus,  Acantholoma,  Aspidolites,  Dis- 
cranurus. 

Champernowne  (A.)  Note  on  a find  of 
Homalonotus  in  Red  Beds  at  Torquay. 

In  Geol.  Mag.,  new  series,  decade 2,  vol.  8, 
1881,  p.  487. 

Chapman  (E.  J.)  Asaphus  canadensis. 

In  Canadian  Jour.,  new  series,  vol.  1,  1856, 
p. 482. 

A review  of  the  Trilobites,  their 

characters  and  classification. 

In  Canadian  Jour.,  new  series,  vol.  1, 1856,  p. 
271,  wood-cuts. 

Trinucleus  concentricus. 

Iu  Canadian  Jour.,  new  series,  vol.  3,  1858, 
p.  414,  wood-cut. 

On  some  new  Trilobites  from  Cana- 
dian rocks. 

In  Annals  Mag.  Nat.  Hist.,  3d  series,  vol„2, 
1858,  p.  9,  2 figs. 

Asaphus  canadensis,  A.  halli. 

On  some  new  Trilobites  from  Cana- 
dian rocks. 

In  Canadian  Jour.,  new  series,  vol.  3,  1858,  p. 
230,  2 wood-cuts. 

Asaphus  canadensis,  A.  halli. 

On  the  hypostoma  of  Asaphus  cana- 
densis and  on  a third  new  species  of 
Asaphus  from  the  Canadian  rocks. 

In  Canadian  Jour.,  new  series,  vol.  4,  1859, 
p.  1,  2 figs. 

Asaphus  canadensis,  A.  hincksii. 

On  the  probable  nature  of  the  sup- 
posed fossil  tracks  known  as  Protich- 
nites , etc. 

In  Canadian  Jour.,  new  series,  vol.  16,  1877, 
p.7. 

Clarke  (J.  M.)  New  Pliyllopod  Crusta- 
ceans from  the  Devonian  of  western 
New  York. 

In  Am.  Jour.  Sci.,  3d  series,  vol.  23,  1882,  p. 
476,  plate. 

Estheria,  Spathiocaris  n.  g.,  Lisgocaris  n.  g. 


[BULL.  63. 


22  A BIBLIOGRAPHY  OF  PALEOZOIC  CRUSTACEA. 


Clarke  (J.  M.)— Continued. 

Girriped  Crustacean  from  the  De- 
vonian. 

In  Am . J our.  Sci.,  3d  series,  vol.  24, 1882,  p.  55. 

Plumulites  devonicus. 

New  discoveries  in  Devonian  Crus- 
tacea. 

In  Am.  Jour.  Sci.,  3d  series,  vol.  25,  1883,  p. 

120. 

Dipterocaris  n.  g. 

Ueber  deutsclie  oberdevonische 

Crustaceen  (hierzu)  Tafel  4. 

In  Neues  Jalirbuch  fur  Mineral.,  1884,  pt.  1, 
p.  178. 

Spathiocaris,  Entomis,  Dithyrocaris. 

On  the  higher  Devonian  fauna  of 

Ontario  County,  New  York. 

In  Bull.  U.  S.  Geol.  Survey,  No.  16, 1885,  3 pis. 

Ceratiocaris,  Beyrichia,  Echinocaris,  Spathio- 
caris. 

The  structure  and  development  of 

the  visual  area  in  the  Trilobite  Phacops 
rana  Green. 

In  Jour.  Morphology,  vol.  2,  No.  2,  Nov.,  1888, 
Boston,  pif253,  pi.  21. 

Clarke  (W.  B.)  On  the  occurrence  of 
Trilobites  in  New  South  Wales. 

In  Quart.  Jour.  Geol.  Soc.  London,  vol.  4, 1848, 
p.  63  (not  descriptive). 

Claypole  (E.  W.)  Note  on  a large  Crus- 
tacean from  the  Catskill  group  of 
Pennsylvania. 

In  Proc.  Am.  Philos.  Soc.,  Phila.,  vol.  21, 1883, 
p.  236,  plate. 

Dolichocephala  n.  g. 

On  the  occurrence  of  the  genus  Dal- 

manites  in  the  Lower  Carboniferous 
rocks  of  Ohio. 

In  Geol.  Mag.,  decade  3,  vol.  1,  London,  1884, 
p.  303. 

Dalmanites?  cuyahogce. 

Conrad  (T.  A. ) Report  on  the  Palaeonto- 
logical Department. 

In  Kept.  Geol.  Survey  New  York,  1838,  p.  107. 

Platynotus  n.  g. 

On  the  Silurian  system ; with  a table 

of  the  strata  and  characteristic  fossils. 

In  Am.  Jour.  Sci.,  1st  series,  v<Jl.  38, 1840,  p.  86. 

Third  Anuual  Report  on  the  Palae- 
ontological Department  of  the  Survey. 

In  Kept.  Geol.  Survey  New  York,  1840,  p.  199. 

Odontocephalus  n.  g.,  Acanihaloma  n.  g., 
Odontocephalus  selenurus , Asaphus  halli, 
Acidaspis  tuberculatus. 

Description  of  new  genera  and  spe- 
cies of  organic  remains.  Crustacea. 

In  Rept.  Geol.  Survey  New  York,  1841,  p.  48, 

lpl. 


Conrad  (T.  A.) — Continued. 

Aspidolites  n.  g.,  Dicranurus  n.  g.,  Asaphus ? 
acantholeurus , A.?  denticulatus , A.  nasutus, 
A.  aspectans,  Calymene-senaria. 

The  plate  accompanying  this  report  was 
distributed  with  a few  copies.  Republished  in 
the  15th  Rept.  New  York  State  Cab.  Nat.  Hist., 
pi.  11. 

Cytherinaalta. 

In  Geol.  Survey  New  York,  pt.  3,  comprising 
the  survey  of  the  3d  Geol.  Dist.  (Vanuxem), 
1842,  p.  112,  fig.  23,  No.  6. 

Observations  on  the  Silurian  and 

Devonian  systems  of  the  United  States, 
with  descriptions  of  new  organic  re- 
mains. 

In  Jour.  Acad.  Nat.  Sci.,  Phila.,  vol.  8, 1842,  p. 
228,  6 pis. 

Asaphus corycosus,  A.  ? trentonensis,  Calymene 
spinifera,  G.  earner ata,  Dipleura. 


Observations  on  the  lead-bearing 

limestone  of  Wisconsin,  and  descrip- 
tions of  a new  genus  of  Trilobites  and 
fifteen  new  Silurian  fossils. 

In  Proc.  Acad.  Nat.  Sci.  Phila.,  vol.  1,  1843,  p. 
329. 

Thaleops  n.  g. 

Corda  (A.  J.  C.)  and  Hawle  (Ignaz). 
Prodrom  einer  Monographie  der  bohmi- 
schen  Trilobiten. 

In  Abhandl.  bohm.  Gesell.  "Wiss.,  Prag,  vol.  5, 
1847,  pp.  129-292,  7 pis. 

This  work  is  generally  attributed  to  A.  J.  C. 
Corda.  The  58  new  genera  described  in  this 
work  are  arranged  by  Joachim  Barrande,  Sys- 
teme  silurien  du  centre  de  la  Boheme,  vol.  1, 
p.  39,  as  follows : 


I.  Division.  Telejurides. 


Phhysacium  i 


= Hydrocephalus  Barr. 


S ==  Sao  Barr. 


Phanoptes  5 
Crithias 
Tetracnemis 
Goniacanthus 
Enneacnemis 
Acanthocnemis 
Acanthogramma 
Eudogramma 
Micropyge 
Selenosema 
Staurogmus  j 
Herse 
Agraulos 
Conocoryplie  1 

Ptychoparia  )•  = Conocephalus  Zenk. 
Ctenocephalus.  j 
Selonopeltis=  Acidaspis  Murch. 
Polytomurus  = Dionide  Barr. 
Tetrapsellium  — Trinucleus  Lhwyd. 
Phalacroma=  Agnostus  (in  part)  Brong. 
Selenoptyclius  = iEglina  Barr. 
Mesospheniscus  = Agnostus  integer  Beyr. 
Diplorrhina  = Agnostus  integer. 


| = Arionellus 


Barr. 


VOGDES.] 


LIST  OF  AUTHORS. 


23 


Corda  (A.  J.  C.)  and  Hawle  (Ignaz) — 
Continued. 

I.  Division.  Telejurides— Cont’d. 


25.  Condylopyge  ) _ ^gnog^us  rex  Barr. 

26.  Lejopyge  3 

27.  Microparia  = JEglina  Barr. 

28.  Pl8esiacomia  = I]l8enu3  Dalm. 

29.  Cyclopvge=iEglina  (in  part)  Barr. 

30.  Alceste  = Illaenus  (in  part)  Dalm. 

31  Xiphogonium  = Proetus  Stein. 

32.  Conoparia  = Cyphaspis  Burin. 

33.  Goniopleura  — Proetus  elegantulus  Ang. 

34.  Aulacopleura  = Arethusina  Barr. 

35.  Pharostoma  = Calymene  Brong. 

^ra®toPJse  ^ = Dalmania  (in  part)  Emmrkh. 
37.  Odontoeliile  3 ^ 

(This  generic  term  was  used  in  1834  for  a genus 
of  the  Coleoptera). 


II.  Division.  Odonturides. 

38.  Amphytrion  ==Remopleurides  Portlock. 

39.  Artlirorhachis  = Agnostus  tardus  Barr. 

40.  Peronopsis  = Agnostus  integer  Beyr. 

41.  Battus  = Agnostus  integer. 

42.  Pleuroctenium‘=  Agnostus  granulatus  Barr. 

43.  Thysanopeltis  = Bronteus  (in  part)  Gold. 

44.  Dind>mene  = Bindymene  Corda. 

, „ . . . c Proetus  (in  part)  Stein. 

45.  Pnonopelt.s=  ptiEtoIliae3  Barr. 


46. 

47. 

48. 


50. 

51. 

52. 

53. 

54. 


56. 


58. 


Asteropyge  ) __  j)a^mania  (}n  part)  Dalm. 
Metacanthus  3 

Odontopyge  = Olenus  spinulosus. 
Placoparia  = Placoparia  Corda. 
Eccoptochile  = Cheirurus  Beyr. 
Actinopeltis  = Cheirurns  Beyr. 

Trochurus  = Staurocephalus  Barr. 
Corydocophalus 
Dicranopeltis 
Acanthopyge 
Dicranogmus  J 
Trapelocera  = Acidaspis  Murch. 
Ceratopyge=  Olenus  forficnla  Sars. 


Cozzens  (Issachar).  Description  of  three 
new  fossils  from  the  Falls  of  the  Ohio. 

In  Annals  Lyceum  Nat.  Hist.  «New  York, 
vol.  4,  1846,  p.  157,  1 pi. 

Piliolites  n.  g. 

The  author  therein  describes  a species  of 
Proetus  under  the  name  of  Piliolites  ohioensis. 


Da  Costa  (E.  M.)  A letter  concerning 
the  fossil  from  Dudley. 

In  Philos.  Trans.  Royal  Soc.,  vol.  48,  pt.  1,  No. 
42,  1753,  p.  286,  pi.  1,  figs.  6-8. 

Dr.  Da  Costa  herein  gives  the  name  of  Pedi- 
cuius  marimns  major  trilobus  to  the  then  called 
Dudley  fossils  ( Calymene  blumenbachii) , and 
declares  it  to  be  a crustaceous  animal  nearly 
related  to  the  living  Isopodes. 


Description  of  a curious  fossil  ani- 

mal. 

In  Gentleman’s  Mag.,  vol.  25,  London,  1754,  p. 
24,  pi.  — , fig.  3. 

Calymene  blumenbachii. 


I Dalman(J.W.)  N&grapetrificater  fundne 
i Ostergotlands  ofvergangskalk  after- 
knade  och  beskrifne. 

In  Svenska  Vetensk.  Akad.  Handl.,  1824,  p. 
368,  pi.  4. 

Entomostr.  actinurus. 

Om  Palseaderna  eller  de  sa  kallade 

Trilobiterna.  Stockholm,  1826, 6 pis. 

Svenska  Vetensk.  Akad.  Handl.,  1826,  p.  226. 

The  German  translation  bears  the  following 
title:  Ueber  die  Palseaden,  oder  die  sogenann- 
ten  Trilobiten  von  J.  D.  Dalman,  von  Friedrich 
Engelhart,  mit  6 Kupfertafeln,  Niirnberg,  1828. 

Dalman  arranges  41  species  of  Trilobites 
under  5 genera  and  4 subgenera,  as  follows : 

Division  I.  Oculated:  1st  genus,  Calymene ; 
2d  genus,  Asaphus. 

Division  II.  Typhlini : 3d  genus,  Ogygia;  4th 
geuus,  Olenus  ( Paradoxides  Br.).  Section  2. 
Battoides : 5th  genus,  Battus  (Agnostus  Br.). 

Subgenera:  1.  Asaphus  ( Nileus );  2.  Asaphus 
(Illcenus) ; 3.  Asaphus  (Ampyx) ; 4.  Lichas  n.  g. 

Arsberattelse  om  nyare  zoologiska 

arbeten  och  upptackter. 

This  work  forms  a part  of  the  annual  report 
of  the  keepers  of  the  Swedish  State  Museum 
for  1828.  It  contains  (p.  134),  under  the  title  of 
“Nya  Svenska  Palaeades”  a description  of  the 
following  Trilobites:  Calymene  ornata,  C.  ver- 
rucosa, C.  clavifrons,  C.?  centrina,  Asaphus 
heros,  A.  platynotus,  Nileus  qlomerinus , Ampyx 
pachyrrhinus,  Battus  Icevigatus,  B.  pisiformis. 

Nouvelles  especes  de  Trilobites  ou 

Paheades  de  Suede. 

In  Bull.  Ferussac,  vol.  19,  1828,  p.  129. 

A notice  of  the  preceding  reference. 

Dames  (W.)  Ueber  Hoplolichas  und  Cono- 
lichas , zwei  Untergattungen  von  Lichas. 

In  Zeitschr.  Deutsch.  geol.  Gesell.,' Berlin, 
1877,  vol.  29,  pt.  1,  p.793,  3 pis. 

The  type  used  for  the  new  genus  Hoplolichas 
is  Lichas  tricuspidatus  Boll,  and  for  Conolichas, 
Lichas  asquiloba  Steinh. 

Geologische  Reisenotizen  aus  Schwe- 

den. 

In  Zeitschr.  Deutsch.  geol.  Gesell.,  Berlin, 
1881,  vol.  33,  p.  405. 

Paradoxides  celandicus,  P.  tessini,  P.  forch- 
hammeri,  P.  kjerulfi,  Ellipsocephalus , Lichas, 
Megalaspis,  Asaphus?,  Agnostus. 

Erste  Abhandlung.  Cambrische 

Trilobiten  von  Lian  Tung,  China 
(Richthofen).  Vol.  4.  Berlin,  1883, 
pis.  1,2. 

The  author  suggests  the  new  generic  term 
Dorypyge  for  certain  Trilobites  which  have  the 
pygidium  armed  with  strong  spines,  thepennb 
timate  pair  being  the  longest,  including  in  the 
genus  Dikelocephalus  quadriceps  Hall  and  Whit- 
field and  D.  gothicus  Hall  and  Whitfield. 


24 


A BIBLIOGRAPHY  OF  PALEOZOIC  CRUSTACEA. 


[BULL.  63. 


Dames  (W.) — Continued. 

Under  Anomocare  Angelin  he  includes  the 
following  American  species : Conocephalites 

hamulus  Owen,  C.  wisconsinensis  Owen,  and 
C.  patter soni  Hall. 

Conocephalites  frequens,  C.  quadriceps , C.  ty- 
pus,  C.  subquadratus,  Anomocare  latelimbatum, 
A.  minus,  A.  planum,  A.  nanum,  A.  majus,  A. 
subcostatxim,  Liostracus  talingensis,  L.  megalu- 
rus , Dorypyge  n.  g.,  D,  richthofeni,  Agnostus 
chinen. 

E.  W.  Claypole : On  the  occurrence 

of  the  genus  Dalraauites  in  the  Lower 
Carboniferous  rocks  of  Ohio.  Geol. 
Mag.  London,  1884. 

In  Neues  Jahrbuch  fur  Mineral.,  1885,  vol. 
1,  p.  102  (abstract). 

Dalmanites,  Phillipsia,  Proetus. 

C.  D.  Walcott:  Appendages  of  the 

Trilobites.  Science,  vol.  3.  1884,  p.  279. 

In  Neues  Jahrbuch  fur  Mineral.,  vol.  1,  p. 
102  (abstract). 

Asaphus , Calymene,  Ceraurus. 

T.  R.  Jones  and  J.  W.  Kirkby:  On 

some  Carboniferous  Entomostracafrom 
Nova  Scotia.  Geol.  Mag.  London,  1884. 

InNeqps  Jahrbuch  fur  Mineral.,  vol.  1, 1885, 
p.  106  (abstract). 

Leperditia,  Beyrichia. 

T.  R.  Jones  and  H.  Woodward : 

Notes  on  Phyllopdiform  Crustacea,  re- 
ferable to  the  genus  Echinocaris  from 
the  Palaeozoic  rocks.  Geol.  Mag.  Lon- 
don, 1884. 

In  Neues  Jahrbuch  fur  Mineral.,  vol.  1, 1884, 
p.  110  (abstract). 

Chas.  E.  Beecher : Ceratiocaridae 

from  the  Chemung  and  Waverly  group 
of  Warren  County.  Second  Geol.  Sur- 
vey, Penn.  Rept.  PPP. 

In  Neues  Jahrbuch  fur  Mineral.,  vol.  1, 1884, 
p.  110  (abstract). 

■ J.  Mickleborough : Locomotory  ap- 

pendages of  Trilobites.  Geol.  Mag. 
London,  1884. 

In  Neues  Jahrbuch  fur  Mineral.,  1885,  p.  477. 

F.  Schmidt  and  T.  R.  Jones:  On 

some  Silurian  Leperditia.  Annals  Nat. 
Hist.,  series  5,  vol.  9,  1882,  p.  168. 

In  Neues  Jahrbuch  fiir  Mineral.,  1885,  vol.  It 
p.  105  (abstract). 

Dana  (James  D. ) Trilobites  in  the  Pots- 
dam sandstone. 

In  Edinburgh  New  Philos.  Jour.,  vol.  6, 1857, 
p.  350. 

On  the  supposed  legs  of  Trilobites 

( Asaplius  platycephalus). 

In  Annals  Nat.  Hist.,  4th  series,  vol.  7,  Lon- 
don. 1871,  p.  366;  Am.  Jour.  Sc.,  3d  seiies  vol. 
1,  1871,  p.  320. 


Dana  (James  D.)— Continued. 

Manual  of  geology,  treating  of  the 

principles  of  the  science  with  special 
reference  to  American  geological  his- 
tory. 2d  ed.  New  York,  1874,  p.  174. 

D’Archiac  (A.)  and  Verneuil  (E.  de). 
On  the  fossils  of  the  older  deposits  in  the 
Rhenish  Provinces,  preceded  by  a gene- 
ral survey  of  the  fauna  of  the  Palaeozoic 
rocks,  and  followed  by  a tabulated  list 
of  the  fossils  of  the  Devonian  system  of 
Europe. 

In  Bull.  Soc.  G6ol.  France,  vol.  13,  1841— ’42 ; 
Trans.  Geol.  Soc.  Lond.,  vol.  6,  pt.  2, 1842,  p.  303. 

, Fischer  (de  Waldheim  G.)  and 

Verneuil  (E.  de).  Pal&mtologie  de 
PAsie  Mineure.  Paris,  1866,  atlas,  21 
pis.  (*) 

Dawson  (J.  W.)  On  the  Lower  Coal 
Measures  as  developed  in  British 
America. 

In  Quart.  Jour.  Geol.  Soc.  London,  vol.  15, 
1859,  p.  62. 

Tracks  of  a Crustacean. 

Note  on  the  fossils  of  Nova  Scotia. 

In  Canadian  Naturalist,  vol.  5,  1860.  p.  297 
(wrongly  paged  197  in  the  volume). 

Homalonotus  dawsoni  Hall. 

On  the  foot  prints  of  Limulns  as  com- 
pared with  the  Protichnitts  ol  the  Pots- 
dam sandstone. 

In  Canadian  Naturalist,  vol.  7,  1862,  p.  271 
Am.  Jour.  Sci.,  2d  series,  vol.  34, 1862,  p.  416. 

Acadian  geology.  The  geological 

structure,  organic  remains,  and  mineral 
resources  of  Nova  Scotia,  New  Bruns- 
wick, and  Prince  Edward  Island,  etc. 
London. 

Three  editions,  1855-’78  (3d  ed.  contains  the 
supplement  to  the  2d  ed.). 

Paradoxides , Conocephalites,  Phillipsia,  Dal- 
manites, Agnostus,  Microdiscus. 

Mr.  C.  F.  Hartt’s  descriptions  of  the  trilo- 
bites first  appeared  in  the  third  edition  of  this 
work.  The  original  MSS.  described  Micro- 
discus dawsoni  under  the  new  generic  name  of 
Dawsonia,  but  on  Prof.  E.  Billings’s  authority 
the  author  has  referred  it  to  Microdiscus  daw- 
soni. 

Eurypterus,  Estheria,  Leaia,  Beyrichia,  Le- 
perditia, Cythere , Diplostylus. 

Supplement  to  the  2d  edition  of 

Acadian  geology.  Containing  addi- 
tional facts  as  to  the  geological  struct- 
ure, fossil  remains,  and  mineral  re- 
sources of  Nova  Scotia,  New  Brunswick, 
and  Prince  Edward  Island.  London, 

| 1878. 


VOGDES.] 

Dawson  (J.  W.) — Continued. 

Homalonotua  dawsoni,  Protirhnites  carbo- 
narius , Anthracopalcemon  ( Palceocarbus ) hil- 
lianum. 

Note  on  two  Palaeozoic  Crustaceans 

from  Nova  Scotia. 

In  Geol.  Mag.,  decade  2,  vol.  4,  London,  1877, 
p.  56.  (See,  also,  Supplement  Acadian  Geol., 
1878,  p.  55,  fig.  10.) 

Anthracopalcemon  (Palceocarabus)  hillianum, 
Homalonotus  dawsoni. 

Day  (F.  H.)  On  the  fauna  of  the  Niagara 
and  Upper  Silurian  rocks  as  exhibited 
in  Milwaukee  County,  Wisconsin,  and 
in  counties  contiguous  thereto. 

In  Trans.  Wisconsin  Acad.  Sc.,  vol.  4,  1876- 
*77,  p.  113. 

Dekay  ( J.  E. ) Observations  on  the  struc- 
ture of  Trilobites,  and  description  of  an 
apparently  new  genus;  with  notes  on 
the  geology  of  Trenton  Falls,  by  James 
Renwick.  Read  Nov.  22  (1824). 

In  Annals  Lyceum  Nat.  Hist.,  New  York,  vol. 
1,  1824.  p.  174,  2 pis. ; Isis  (oder  Encycl.  Zeit- 
ung),  Oken,  1825  and  1832. 

Isotelus  n.  g. 

Observations  on  a fossil  crustaceous 

animal  of  the  order  Branchiopoda. 
Read  Dec.  12,  1825. 

In  Annals  Lyceum  Nat.  Hist.,  New  York,  vol. 
1,  pt.  2,  p.  375,  pi.  29.  Republished  in  Harlan’s 
Med  Phys.  Researches,  1835,  p.  297. 

Eurypterus  n.  g. 

Report  on  several  fossil  raultilocular 

shells  from  the  State  of  Delaware;  with 
observations  on  a second  specimen  of 
the  new  fossil  genus  Eurypterus.  Read 
Oct.  2,  1827. 

In  Annals  Lyceum  Nat.  Hist.,  New  York, 
vol.  2,  1828,  p.273. 

Deslongchamps  (E.)  M^moire  sur  les 
corps  organises  fossiles  du  gr&s  inter- 
mddiaire  du  Calvados. 

In  Soc.  Linn.  Calvados,  vol.  2,  1825,  p.  291,  2 
pis. 

The  author  herein  describes  two  species  of  the 
genus  Homalonotus  under  the  names  Asaphus 
brongniarti  and  A.  brevicaudatus. 

Dethleff  (von)  and  Boll  (Ernst).  Die 
Trilobiten  Mecklenburgs. 

In  Arcbiv  Vereins  Freunde  Naturg.  Mecklen- 
burg, 1858,  p.  155. 

Remopleurides , Paradoxides,  Ellipsocephalus, 
Olenus,  O.  ( Sphcerophthalmu8 ),  Proetus,  Gyphas- 
pis.  Harpides , Phacops,  Galymene,  Uomalono- 
tus,  Licha8.  Trinucleus.  A mpyx , A saphus,  Ogy- 
gin,  IUcenu8.  Nileus,  Acidaspis , Gheirurus, 
Sphcerexochux,  Sphcerocoryphe.  Amphion,  En- 
crinurus,  Bronteus , Telephus,  Holometopus,  Do- 
lichometopus , Agnostus. 


25 

Devine  (T.)  Description  of  a uew  Trilo- 
bite  from  the  Quebec  group. 

In  Canadian  Naturalist,  vol.  8,  1863,  p.  95,  2 
figs. 

Loganellus  n.  g. 

Similar  forms  have  been  referred  by  Corda  to 
the  genus  Ptychoparia. 

Description  of  a new  Trilobite  from 

the  Quebec  group. 

In  Canadian  Naturalist,  vol.  8. 1863,  p.  210,  fig. 

Menocephalus  salteri. 

Dewalque  (G.)  Prodrome  d’une  descrip- 
tion gdologique  de  la  Belgique.  Bru- 
xelles, 1868;  2d  ed.,  1880. 

Contains  important  list  of  fossils,  and  obser- 
vations. 

Dumont  (A.-H.)  M<3moire  sur  la  consti- 
tution g^ologique  de  la  province  de 
Liege. 

In  M6m.  Cour.  Acad.  Roy.  Sci.,  Bruxelles, 
vol.  8,  1832,  p.  353.  Table  of  fossils. 

Durocher  (J.)  Sur  le  test  des  Trilobites 
et  des  auimaux  fossils  de  la  Bretagne 
en  general. 

In  Bull.  Soc.  G6ol.  France,  2d  series,  vol.  7, 
p.  307,  also  vol.  8,  1850-’51,  p.  160. 

Dwight  ( W.  B.  ) Recent  explorations 
in  the  Wappinger  Valley  limestone  of 
Dutchess  County,  New  York. 

In  Am.  Jour.  Sci.,  3d  series,  vol.  27,  1884,  p. 
349,  pi.  7. 

Bathyurus. 

Eaton  (Amos).  Geological  Equivalents. 

Description  of  Ogygies  latissimus  and  Gancer 
trilobioides. 

In  Am.  Jour.  Sci.,  1st  series,  vol.  21, 1832,  pp. 
135, 136,  note. 

Gancer  trilobioides , Oxygies. 

Trilobites. 

Am.  Jour.  Sci.,  1st  series,  vol.  22, 1832,  p.  165. 

Brongniartia  n.  g. 

We  learn  from  reference  to  Dr.  Amos  Eaton’s 
description  and  figures  given  in  his  “Geological 
text-book,”  p.  33,  pi.  1,  fig.  3 (2d  ed.,  1832),  that 
the  original  of  Brongniartia  carcinodea  Eaton 
was  the  same  as  that  afterwards  described  by 
Dr.  Jacob  Green  (Monthly  Am.  Jour  Geology, 
vol.  1,  June,  1832;  also  Mon.  Tril.  N.  A.,  p.  87, 
pi.  1,  fig.  6,  cast  34)  as  Triarthrus  beckii. 

Geological  text-book  for  aiding  the 

study  of  North  American  geology ; be- 
ing a systematic  arrangement  of  facts 
collected  by  the  author  for  his  pupils, 
etc.  2d  ed.,  5 pis.  (June  15,  1832). 

The  following  species  are  described  in  this 
work,  pp.  31-34:  Genus  Galamena,  G.  blumen- 
bachii  (Galymene  smaria  Conrad),  pi.  2,  fig.  19; 
genus  Asaphus,  A.  hansmannii , A.  caudatus 
(Dalmanites  limulurus  Green),  pi.  2,  fig.  18;  A. 
selenourus  (Dalmanites  selenurus  Eaton),  pi.  1, 


LIST  OF  AUTHORS. 


26 


A BIBLIOGRAPHY  OF  PALEOZOIC  CRUSTACEA. 


[BULL.  63. 


Eaton  (Amos) — Continued, 
fig.  1 ; genus  Brongniartia,  B.  platycephala 
( Homalonotus  dekayi  Green),  pi.  2,  fis,  20 ; B. 
isotelea  (Asaphus  platycephalus  Stokes),  pi.  2, 
fig.  22;  B.  carcinodia  ( Triarthrus  becki  Green), 
pi.  1,  fig.  3;  genus  Nuttainiu , N.  concentrica 
(Trinucleus  concentrica  Eaton),  pi.  1,  fig.  2 ; N. 
sparsa  (Homalonotus  dekayi  Green). 

Eichwald  (Eduard).  Observationes  gp- 
ognostico-zoologicse  perlugriam  maris- 
que  Baltici  Provincias  nec  non  de  Trilo- 
bites.  Casani,  1825,  4 pis. 

The  author  herein  describes  and  figures  eight 
species  of  Lower  Silurian  Trilobites  under  the 
new  generic  term  Cryptonymus.  In  his  later 
work  (“Lethoea  Eossica,”  p.  1449)  the  first  three 
are  referred  to  the  genus  Asaphus ; viz,  Crypto- 
nymus schlotheimii  to  Asaphus  schlotheimii, 
Cryp.  weissii  to  Asaphus  weissii,  Cryp.panderi  j 
to  Asaphus  expansus  Wahl.  The  last  five  are  [ 
classed  as  follows : Cryp.  lichtensteinii  under  I 
Niobe  lichtensteinii , Cryp.  rosenbergii  to  Illcenus 
rosenbergii , Cryp.  wahlenbergii  to  Illcenus  wah- 
lenbergii , Cryp.  rudolphii  to  Illcenus  rudolphii , 
Cryp.  parkinsonii  to  Illcenus  parkinsonii. 

This  work  also  contains  a description  and  a 
figure  of  Asaphus  fischeri  (Amphi'on  fischeri 
Eieh*). 

The  description  of  two  new  Carbonic  Trilo-  j 
bites  are  added  by  Dr.  G.  Fischer,  pp.  53-55,  pi. 

4,  figs.  4 and  5,  Asaphus  brongniarti,  pi.  4,  fig.  5. 
and  A.  eichwaldi,  pi.  4,  fig.  4.  Yalerian  von  i 
Moller  ( 1 ‘ Ueber  die  Trilobiten  der  Steinkohlen-  j 
formation  des  Ural,”  1867,  p.  7)  refers  these 
species  to  Phillipsia  eichwaldi  Fisch.,  applying 
the  term  to  the  non-mucronate  pygidium.  The 
Russianmucronate  species,  figured  by  Eichwald 
(“Lethoea  Eossica,”  pi.  54,  fig.  10)  as  Griffith!  \ 
des  eichwaldi , was  assigned  by  the  same  author 
to  Phillipsia  mucronata  McCoy. 

Zoologia  specialis,  quam  expositis 

animalibus  turn  vivis  turn  fossibilibus 
postissernum  Rossise  in  Universum  et  j 
Polonise.  Vilna?,  vols.  1-3,  1829-’31.  (*)  | 

Die  Tbier-  und  Pflanzenreste  des  al- 

ten  rothen  Sandsteins  und  Bergkalk  in 
Novgorodiscben  Gouvernement. 

In  Bull.  Acad.  Petropol.  St.  Petersburg,  vol. 

7, 1840,  p.  78. 

Otarion  eichwaldi. 

Ueber  das  silurische  Scbicbten-Sys- 

tem  von  Ehstland.  St.  Petersburg, 
1840. 

Krustazeen,  p.  64. 

Calymene  odini,  O.  blumenbachii  Brong.,  C. 
downingia  Murch.,  C.  macrophthalma  Murch., 

C. bellatula  Dalm . , C.  sembnitzkii,  Amphion  ( Asa- 
phus) fischeri,  Zethus  verrucosus  Pander,  Cryp- 
tonymus punctatus  (Wahl.)  Eichwald,  C.vario- 
laris,  C.  worthii , Asaphus  expansus  Wahl.,  A. 
weissii,  A.  schlotheimii,  A latus  Pander,  A.  la- 
ceniatus  Dalm.,  A.  dilatatus  Dalm.,  A.  devexus, 


Eichwald  (Eduard)— Continued. 

A.  tyrannus  Murch.,  A.vulcani  Murch.,  Illcenus 
crassicauda  Dalm.,  I.  rosenbergii , I.  coinutus 
Pander,  I.perovatis  Murch.,  I.centrotus  Dalm., 
Trinucleus  sparskii.  Homalonotus  herschelii 
Murch.,  Nileus  armadillo  Dalm.,  Agnostus  na- 
sutus  Dalm. 

Die  Ur  welt  Russlands  durck  Abbild- 

ungen  erlautert. 

4 pts.,  St.  Petersburg,  1840-’48,  14  pis. 

In  the  first  part  of  this  work,  in  the  list  of 
fossils  given,  p.  22,  Eduard  von  Eichwald  re- 
fers three  species  to  Cryptonymus ; a generic 
name  which  he  used  in  1825  for  an  entirely  dif- 
ferent series  of  fossil  Crustacea.  In  t he  present 
work  ho  substitutes  the  name  for  such  species 
as  Calymene  variolaris,  C.  punctatus,  C.worthi, 
etc.  The  name  is  used  without  a generic  de- 
scription, and  only  indicated  by  the  above 
named  species. 

Metopias  n.  g.,  pt.  2,  p.  64,  pi.  3,  fig.  4. 

Beitrage  zur  Geologie  und  Palajon- • 

tologie  Russlands.  Moscau,  1854. 

Bunodes  n.  g. 

Die  Grauwacken  Schichten  von  Liv-  - 

und  Estland. 

In  Bull.  Soc.  Imp.  des  Xaturalistes  Moscou, 
vol.  27,  1854,  no.  1,  p.  3. 

Eurypterus , Pterygotus,  Bunodes,  Sphagodus .? 
Ueber  die  Gattungen  Cryptonymus 
und  Zethus. 

In  Bull.  Soc.  Imp.  des  Naturalistes  Moscou, 
vol.  28, 1855.  Separate  ed.,  Moscou,  1855,  23  pp. 

The  author  maintains  that  the  genus  Cryp- 
tonymus should  be  retained  for  several  Russian 
and  Swedish  Trilobites  as  defined  by  N.  P. 
Angelin  (“Palaeont.  Scand.,”  1852,  p.  2),  with 
Calymene  punctatus  as  its  type. 

Beitrage  zur  geographiseben  Yer- 

breitung  der  fossilen  Tbiere  Russland’s.  ■ : 

In  Bull.  Soc.  Nat.,  Moscou,  vols.  28-30,1855- 
’57  (vol.  30, 1857). 

Harpes,  Proetus,  Cyphaspis,  Homalonotus,  I 
Calymene,  Griffithides,  Phacops,  Chasm  ops,  Odon- 
tochile,  Lichas,  Trinucleus , Ampyx,  Asaphus,  ~ 
Ptychopyge,  Megalaspis,  Nileus,  Illcenus,  Dys- 
planus,  Cheirurus,  Sphcerexochus,  Amphion, 
Cryptonymus , Bronteus,  Loncliodomas,  Itaphia  V 
phorus , Zethus,  Sphcerocoryphe,  Eurypterus, 
Pterygotus , Beyrichia,  Bairdia. 

Letboea  Rossica,  ou  pal(;ontologie  de 

la  Russ.  Stuttgart,  1852-,69.  3 vols.,  j 

with  atlas,  113  pis. 

The  Crustacea  are  arranged  in  the  following 
order:  First  order,  Ostracopouia,  first  family,-*, 
Cypridina,  genus  1.  Leperditia,  2.  Bairdia,  3.  ~ 
Bexjrichia.  Second  order,  Poecilopoda,  second  ; 
family,  Agnostidae,  genus  4.  Agnostus.  Third 
order,  Copepoda,  ! third  family,  Eurypterid®,  , 
genus  5.  Eurypterus , 6.  Pterygotus.  Fourth  \ 
order,  Xiphosurid®,  fourth  family,  Limulid®, 
genus  7.  Campylocephalus  n.  g.  Fifth  order, 
Isopodes,  Trilobites,  family  Harpid®,  genus  9. 


VOGDES.  ] 


LIST  OF  AUTHORS. 


27 


Eichwald  (Eduard*)— Continued. 

Harpes,  10.  Trinucleus,  11.  Ampyx,  12.  Loncho- 
domas,  13.  Raphiophorus ; sixth  family,  Lick  i- 
% dae,  genus  14.  Licltas ; seventh  family,  Chei- 
ruridae,  genus  15.  Acidaspis,  16.  Ceraurus,  17. 

; Sphcerexochus,  18.  Zethus,  19.  Sphcerexocoryphe  ; 
eighth  family,  Amphionidae,  genus  20.  Aviphion, 
21 . Romalonotus,22.  CryptQnymus ; ninth  family, 
Calyminidae,  geuus  23.  Calymene,  24.  Acaste,  25. 
Phacops,  26.  Chasmops,  27.  Proetus,  28.  Griffi- 
thides,  29.  (not  given),  ZQ.Cyphasis;  tenth  lamily, 
Kemopleuridae,  genus  31.  Bunodes,  32.  Pseu- 
u doniscus,  33.  Remopleurides ; eleventh  family, 
Asaphidae,  geuus  34.  Asaphus,  35.  Megalaspis, 
36.  Niobe,  37.  Ptychopyge,  38.  Ogygia,  39.  Illcenus , 
40.  Rhodope , 41.  Dysplanus , 42.  Actinobolus,  43. 
Nileus;  twelfth  family,  Brontid®,  genus  44. 
Bronteus. 

. Beitrage  zur  nahern  Ivenntniss  der 

in  meiner  Lethaea  Rossica  beschrie- 
! benen  Illaenus,  etc. 

In  Bull.  Soc.  Imp.  des  Naturalistes  Moscou, 

' 1863,  No.  4,  p.  372. 

J v Nileus , Bumastus. 

Emerson  (B.  K.)  On  the  geology  of 
Frobisher  Bay  and  Field  Bay. 

Appendix  3.  Narrative  of  the  second  Arctic 
expedition  made  by  Charles  F.  Hall,  45th  Cong., 
3d  sess.,  Senate  Doc.  27,  Washington,  1879. 

Triarthrus,  Cyphaspis,  Phacops,  Calymene, 
Asaphus,  Beyrichia,  Leper ditia,  Primitia. 

Emmons  (Ebenezer).  Geology  of  New 
York.  Pt.  2.  Comprising  the  survey  of 
the  Second  Geological  District.  Al- 
bany, 1842. 

Isotelus  gigas,  fig.  99  (1) ; Bumastus  trenton- 
ensis,  fig.  100  (1) ; Calymene  senaria,  fig.  100  (2) ; 
Illcenus  trentonensis,  fig.  100  (3);  Ceraurus 
pleurexanthus , fig.  100  (6);  Trinucleus  tessellatus, 
fig.  100  (7) ; Triarthrus  beckii,  fig.  110  (1) ; Tri- 
nucleus  caractaci,  fig.  112  (1). 

The  Taconic  system,  based  on  ob- 
servations in  New  York,  Massachusetts, 
Maine,  Vermont,  and  Rhode  Island. 
Albany,  1844,  6 pis.  and  map. 

Atops  trilineatus  n.  s.  and  genus,  fig.  8 ; Ellip- 
tocepala  asaphoides  n.  s.  and  genus  (not  Ellip  - 
socephalus  Zenker,  1833),  fig.  9. 

Agriculture  of  New  York,  comprising 

an  account  of  the  classification,  com- 
position, and  distribution  of  tho  soils 
and  rocks,  etc.  Vol.  1.  Albany,  1846, 
21  pis.  and  maps. 

Atops  trilineatus,  fig.  8;  Elliptocephala  asa- 
phoides, fig.  9. 

On  the  identity  of  the  Atops  trili- 
neatus and  the  Triarthrus  beckii  Green, 
with  remarks  upon  the  Elliptoccphalus 

asaphoides. 


Emmons  (Ebenezer)— Continued. 

In  Proc.  Am.  Assoc.  Adv.  Sci.,  First  meet- 
ing. Philadelphia,  1848. 

Atops  trilineatus,  Triarthrus  beckii,  Elipto- 
cephalus  asaphoides. 

American  geology,  containing  a 

statement  of  the  principles  of  the  sci- 
ence, with  full  illustrations  of  the  char- 
acteristic fossils.  Vol.  1,  Parts  I,  II, 
and  III.  Albany,  1855-57,  atlas,  17  pis. 

Dikelocephalus,  Olenus,  Triarthrus,  Atops, 
Conocephalus,  Elliptocephdlus , Phacops,  Caly- 
mene, Trinucleus,  Isotelus,  Ogygia,  Illcenus, 
Acidaspis,  Ceraurus,  Agnostus,  Microdiscus  n. 
g.,  Beyrichia,  Cytherina,  Cyproides. 

Manual  of  geology,  designed  for  the 

use  of  colleges  and  academies.  New 
'York,  1860. 

Paradoxides?  quadrispinosus , fig.  57;  Para- 
doxides macrocephalus,  fig.  70 ; Atops  punctatus, 
fig.  71;  Microdiscus  quadrico status,  fig.  73; 
Calymene  senaria,  fig.  87 ; Illcenus  trentonensis, 
fig.  89  (a);  Illcenus  crassicauda,  fig.  89  (b);  Tri- 
arthrus beckii,  figs.  89  (c)  and  91 ; Isotelus  gigas, 
fig.  89  (d) ; Beyrichia,  Cytherina , Cyproides,  fig. 
90;  Trinucleus  caractaci,  fig.  93  (1) ; Hemicriptu- 
rus,  fig.  97  (2) ; Illcenus  barriensis  fig.  98  (3) ; 
Dalmania  selenurus,  fig.  118  (1) ; Phacops  bufo, 
fig.  124  (6);  Dalmania  calliteles,  fig.  124  (7); 
Phacops  nupera,  fig.  138  (2) ; Cyphaspis  girarde- 
auensis,  fig.  145  (2) ; Homalonotus  dekayi,  figs. 
134,  135. 

Note  A,  p.  280,  the  author  remarks;  “ We 
now  know  the  following  trilobites,  all  of  which 
belong  to  a slate  beneath  the  Calciferous ; viz, 
Atops  punctatus,  Eliptocephalus  (I’aradoxides) 
asaphoides,  Paradoxides  thompsoni,  P.  vermonti, 
P.  macrocephalus,  Paradoxides  ( Pagura ) qua- 
drispinosus, and  Microdiscus  quadrico  status.” 

Dr.  E.  Emmons  uses  the  name  Pagura  as  a 
subgenus  to  Paradoxides  without  indicating 
his  intention  with  regard  to  the  genus.  He  may 
have  intended  it  to  replace  tho  generic  name 
of  Peltura  ( Olenus ) holopyga  Hall,  12th  Kept. 
New  York  State  Cab.  Nat.  Hist.,  p.  61,  which 
in  the  13th  Rept.  New  York  State  Cab.  Nat. 
Hist.,  p.  118,  is  used  for  the  typo  of  Bathynotus 


Hall,  1860. 

The  preface  of  the  manual  is  dated  Kaleigh, 
May  1,  1859. 


Emmrich  (H.  F.)  De  Trilobitis  disser- 
tatio  petrefactologica  quam  consensu  et 
auctoritate  amplissimi  philosopliorum 
ordinis,  etc.  Berolini,  1839,  1 pi. 

Classifies  65  species  and  9 genera  and  6 sub- 
genera,  as  follows : 

1.  Phacops. 

f Sec.  1.  Ogygia. 

2.  Asaphus. 

3.  Ilhenus. 

4. 


2.  Asaphus 


3.  Calymene 


j Sec.  1.  Calymene. 
t 2.  Trimerus. 


28 


A BIBLIOGRAPHY  OF  PALEOZOIC  CRUSTACEA. 


[bull.  6; 


Emmrich  (H.  F.) — Continued. 

4.  Depleura. 

5.  Conocephalus. 

6.  Ellipsocephalus. 

7.  Ampyx. 

8.  Paradoxides. 

9.  Odontopleura. 

10.  Cyphaeus. 

* Zur  Naturgesehichte  der  Trilobiten. 

Programm  zur  offentlichen  Priifung, 
welclie  mit  den  Zoglingen  der  Real- 
echule  in  Meiningen  Donnerstag  dein 
28.  und  Freitag  den  29.  Marz  1&44  im 
grossen  Horsaale  der  Anstalt  abgehal- 
ten  werden  soil,  etc.  Meiningen,  1844, 
lpl. 

Pt.  1.  Zur  Morphologie  der  Trilobiten,  pp.  4- 
13. 

Pt.  2.  Ueber  die  Trilobiten  gattungen,  pp. 
13-18. 

Pt.  3.  Ueber  die  Verbreitung  der  Trilobiten 
in  den  Gebirgsschichten,  pp.  18-28. 

The  genera  are  arranged  into  25  families  in 
the  following  order : 

1.  Phacops,  Dalmania  n.  g.,  2.  Phillipsia,  3. 
Griffithides,  4.  Gerastos , 5.  Asaphus , 6.  Illcenus, 
7.  Ogygia,  8.  Bronteus,  9.  Nuttama.  10.  Bncri 
nurus  n.  g.,  11.  Amphion,  12.  Calymene,  13.  Ho- 
malonotus,  14.  Conocephalus , 15.  Ellipsocepha- 
lus, 16.  Anthes,  17.  Paradoxides,  18.  Odonto- 
pleura, 19.  Arges,  20.  Cnyptolithus,  21.  Ampyx, 
22.  Olenus , 23.  Remopleurides,  24.  Ceraurus,  25. 
Agnostus. 

Ueber  die  Trilobiten. 

In  Neues  Jahrbuch  fiir  Mineral.,  1845  n 18 
lpl. 

For  list  of  genera,  see  preceding  reference. 

On  the  morphology,  classification, 

and  distribution  of  the  Trilobites. 

Scientific  Memoirs,  edited  by  Richard  Tay- 
lor, vol.  4,  1846,  pt.  14,  p.  253,  1 pi. 

Translation  of  the  preceding  reference. 

E&mark  (H.  M.  T.)  Om  nogle  nye  Arten 
af  Trilob  iter.  (*) 

In  Mag.  for  Naturvidensk.,  andre  Raekke, 
Christiania,  vol.  1,  1833,  p.  268,  pi.  8. 

Trilobiter  asellus,  T.  elliptifrons,  T.  sphoerius , 
T.  semilunaris,  T.  dentatus. 

Etheridge  (Robert).  Description  of  the 
Palaeozoic  and  Mesozoic  fossils  of 
Queensland. 

In  Quart.  Jour.  Geol.  Soc.  London,  vol.  28 
1872,  p.  317. 

GriJJlthides  dubius,  pi.  18,  fig.  7. 

• Memoirs  Geological  Survey  of  Scot- 

land. Edinburgh,  1873. 

Expl.  Map  23,  p.  93. 

Ceratiocaris. 

■ Observations  on  a few  Graptolites 

from  the  Lower  Silurian  rocks  of  Vic- 


J Etheridge  (Robert) — Continued. 

toria,  Australia,  with  a further  note  o: 
the  structure  of  Ceratiocaris. 

In  Annals  Mag.  Nat.  Hist.,  London,  4th  s< 
ries,  vol.  14,  1874.  p.  1. 

On  the  remains  of  a large  Crustacea] 
probably  indicative  of  a new  species  o: 
Eurypteridw,  or  allied  genus  (Eurypteru, 
stevensoni),  from  the  Lower  Carbonifer 
ous  series  (Cementstone  group)  of  Ber 
wickshire. 

In  Qiiart.  Jour.  Gcol.  Soc.  London,  vol.  33 

1877,  p.  223,  2 figs. 

Palaeontology  of  the  coasts  of  the 

Arctic  lands  visited  by  the  late  Brit- 
ish expedition  under  Capt.  Sir  George 
Mares,  etc. 

In  Quart.  Jour.  Geol.  Soc.  London,  vol.  34 

1878,  p.  568. 

Proetus , Calymene,  Asaphus,  Encrinurus 
Bronteus. 

On  the  occurrence  of  the  genui 

Dithyrocaris  in  the  Lower  Carbonifer- 
ous or  Calciferous  sandstone  series  of 
Scotland,  and  on  that  of  a second  spe- 
cies of  Anatlirapaloemon  in  these  beds. 

In  Quart.  Jour.  Geol.  Soc.  London,  vol.  35, 

1879,  p.  464,  pi.  23. 

Dithyrocaris,  Anthrapalcemon. 

On  the  occurrence  of  a small  new 

Phyllopod  Crustacean,  referable  to  the 
genus  Leaia  in  the  Lower  Carbonifer- 
ous rocks  of  Edinburgh. 

In  Annals  Mag.  Nat.  Hist.,  London,  5th  se- 
ries, vol.  3,  1879,  p.  257. 

and  Nicholson  (H.  A. ) See  Nichol-  i 

son  (H.  A.)  and  Etheridge  (Robert).  I 

and  Salter  (J.  W.)  See  Salter  (J. 

W.)  and  Etheridge  (Robert). 

Notes  on  a collection  of  fossils  from  I 

the  Palaeozoic  rocks  of  New  South 1 
Wales. 

In  Proc.  Royal  Soc.  New  South  Wales,  vol. 
19, 1880,  p.  247,  1 pi. 

Encrinurus  punctatus. 

Address  of  the  President. 

In  Quart.  Jour.  Geol.  Soc.  London,  vol.  37, 
1881,  p.  37. 

Reports  of  the  committee,  consisting 

of  Mr.  R.  Etheridge,  Dr.  Henry  Wood-  jj 
ward,  and  Prof.  T.  Rupert  Jones,  sec-  i 
retary,  on  the  fossil  Phyllopoda  of  the 
Palaeozoic  rocks. 

See  Reports  of  the  secretary,  recorded  under 
Jones  (T.  Rupert).  See,  also,  Woodward 
(Henry)  and  Etheridge  (Robert) ; Huxley  (T. 
H.)  and  Etheridge  (Robert). 


iGDES.J 


LIST  OF  AUTHORS. 


29 


theridge,  jr.  (Robert).  On  the  occur- 
rence of  a raacrurous  decaped  ( Anthra - 
plcemon  woodwardi  sp.  nov.)  in  the  Red 
Sandstone  or  lowest  group  of  the  Car- 
boniferous formation  of  the  southeast 
of  Scotland. 

In  Quart,  Jour.  Geol.  Soc.  London,  vol.  33, 
1877,  p.  863,  pi.  27. 

— On  Pinnocaris  lapworthi. 

Proc.  Royal  Phys.  Soc.,  1878,  vol.  4,  p.  167. 
Pinnocaris  n.  g. 

— On  the  genus  Conocephalites. 

In  Proc.  Royal  Soc.  Tasmania,  June,  1882,  p. 
152. 

’eistmantel  ( Ottokar ).  Ueber  ein  neues 
Vorkommen  von  nordischen  silurischen 
Diluvilgeschieben  bei  Lampersdorf  in 
der  Grafschaft  Glatz  (Zeitschrift  Lotos, 
Dec.,  1874,  p.  10,  Prag). 

Phacops  downingice,  Leperditia  marginata. 
Fischer  (G.  de  Waldheim).  Notice  sur 
l’Eurypterus  de  Podolie  et  le  Chiro- 
therium  de  Livonie.  Moscou,  1839,  2 
pis. 

JEurypterus  remipes,E.  lacustris?,  E.  tetra- 
gonoijhthalmus  n.  s. 

Pitch  (Asa).  Fossils  of  Washington 
County,  New  York. 

In  Trans.  New  York  Agric.  Soc.,  vol.  9, 1850, 

p.  862. 

Atops  trilineatus , Olenus  asaphoides,  Trinu- 
cleus concentrica. 

Fletcher  (W.  F.)  Observations  on  Dud- 
ley Trilobites. 

In  Quart.  Jour.  Geol.  Soc.  London,  vol.  6, 1850, 
p.  235,  pis.  27,  27  bis. 

IAchas  bucklandi,  L.  hirsutus,  L.  grayii,  L. 
salteri,  L.  barrandii. 

Observations  on  Dudley  Trilobites. 

Part  2. 

In  Quart.  Jour.  Geol.  Soc.  London,  vol.  6, 1850, 
p.  402.  pi.  32. 

Cybele  punctata,  C.  variolaris. 

Poerste  (A.  F.)  The  Clinton  group  of 
Ohio. 

In  Bull.  Denison  Univ.,vol.  1, 1885,  p.  65,  2 pis. 
Acidaspis  Bathyurus?,  Illcenus,  Calymene , 
Lichas,  Arionellus?,  Dalmanites. 

The  Clinton  group  of  Ohio.  Pt.  2. 

In  Bull.  Denison  T7niv.,vol.  2, 1887,  p.  89,  pi.  8. 
Proetus,  Phacops,  Dalmanites,  Calymene, 
Lichas,  Illcenus,  Acidaspis,  Ceraurus,  Encri- 

nurus. 

Note  on  Ilkeni. 

In  Fifteenth  Rept.  Geol.  Nat.  Hist.  Survey 
Minnesota,  1886,  p.  478. 

lUcenus  minnesotensis,  I.  herricki,  I.  ambi- 
gnus,  I.  insignis  Hall. 


Foerste  (A.  F.) — Continued. 

Notes  on  Palaeozoic  fossils.  Pt.  2. 

In  Bull.  Denison  Univ.,  vol.  3,  pt.  2,  1888,  p. 
117,  pi.  13. 

Phacops,  Lichas,  Sphcerexochus,  Encrinurus , 
Microdiscus. 

Forbes  (Edward).  Description  of  Ampyx 
nudus. 

In  Mem.  Geol.  Survey  United  Kingdom,  de- 
cade 2,  London,  1849,  pi.  2. 

Ampyx  nudus,  Bracharnpyx  n.  g. 

Ford  (S.  W.)  Description  of  some  new 
species  of  Primordial  fossils. 

In  Am.  Jour.  Sci.,  3d  series,  vol.  3,  1872,  p. 
419. 

Agnostus  nobilis. 

Descriptions  of  new  species  of  fos- 
sils from  the  Lower  Potsdam  group  at 
Troy,  New  York. 

In  Am.  Jour.  Sci.,  3d  series,  vol.  6, 1873,  p.  137. 

Microdiscus  speciosus,  Leperditia  troyensis. 

Note  on  the  discovery  of  a new  local- 
ity of  Primordial  fossils  in  Rensselaer 
County,  New  York. 

In  Am.  Jour.  Sci.,  3d  series,  vol.  9, 1875,  p.  204. 

Conocephalites  (Atops)  trilineatus  Emmons. 

On  additional  species  of  fossils  from 

the  Primordial  of  Troy  and  Lansing- 
burg,  Rensselaer  County,  New  York. 

In  Am.  Jour.  Sci.,  3d  series,  vol.  11, 1876,  p.  369. 

Microdiscus  meeki. 

Note  on  Microdiscus  speciosus. 

In  Am.  Jour.  Sci.,  3d  series, vol.  13, 1877,  p.  141. 

On  some  embryonic  forms  of  Trilo- 
bites. 

In  Am.  Jour.  Sci.,  3d  series,  vol.  13, 1877,  p. 
265,  pi.  4. 

Metamorphoses  of  Olenellus  ( Elliptocephalus ) 
asaphoides. 

Description  of  two  new  species  of 

Primordial  fossils. 

In  Am.  Jour.  Sci.,  3d  series,  vol.  15, 1878,  p.  124. 

Solenopleura  nana. 

Note  on  the  development  of  Olenellus 

asaphoides. 

In  Am.  Jour.  Sci.,  3d  series,  vol.  15, 1878,  p.  129. 

Life  of  the  Silurian  age. 

New  York  Tribune  Extra,  September 2, 1879. 

In  this  paper  Mr.  S.  W.  Ford  gives  generic 
figures  of  Trilobites,  including  figures  of  Mi- 
crodiscus speciosus. 

Note  on  the  Trilobite  Atops  trilinea~ 

tus  Emmons. 

In  Am.  Jour.  Sci.,  3d  series,  vol.  19, 1880,  p.  152. 

On  additional  embryonic  forms  of 

Trilobites  from  the  Primordial  rocks  of 
Troy,  New  York,  with  observations  on 


30 


A BIBLIOGRAPHY  OF  PALEOZOIC  CRUSTACEA, 


[bull.  63. 


Ford  (S.  W.) — Continued, 
the  genera  Olenellus , Paradoxides,  and 
Hydrocephalus. 

In  Am.  Jour.  Sci.,  3d  series,  vol.  22, 1881,  p.  250, 
13,  figs. 

Note  on  the  age  of  the  Swedish  Para- 
doxides beds. 

In  Am.  o our.  Sci.,  3d  series,  vol.  32, 1886,  p.  473. 

and  Dwight  (W.  B.)  Preliminary 

report  of  S.  W.  Ford  and  W.  B.  Dwight 
upon  fossils  obtained  in  18*5  from  meta- 
morphic  limestones  of  the  Taconic 
series  of  Emmons,  at  Canaan,  New 
York.  PI.  7. 

In  Am.  Jour.  Sci.,  3d  series,  vol.  31, 1886,  p.  248. 

Genal  spine  of  Trilobite,  perhaps  Asaphus 
megistos. 

Freeh  (Fritz)..  Ueber  das  Devon  der 
Ostalpen. 

In  Zeitschr.  Deutsch.  geol.  Gesell.,  Berlin, 
vol.  39,  1888,  p.  659. 

Phacops , Cheirurus,  Encrinurus,  Arethusina. 

Die  palaozoischen  Bildungen  von 

Cabrieres,  etc. 

Inr  Zeitschr.  Deutsch.  geol.  Gesell.,  Berlin, 
vol.  39,  1887,  p.  360,  pi.  24. 

Harpes,  Phacops , Proetus,  Dechenella,  Lichas, 
Cheirurus,  Bronteus,  Ogygia. 

Gehler  ( J.  C. ) De  quibusdam  varioribus 
agri  Lipsiensis  petrificatis.  Spec.  I. 
Trilobites  f.  Entomoslithus  paradoxus 
Linnd.  Lipshe,  1793  [1  pi.]. 

The  author  gives  a sketch  of  the  bibliography 
of  the  Trilobites,  and  figures  several  specimens 
of  Calymene  blumenbachii. 

Geinitz  (H.  B.)  Grundriss  der  Verstei- 
nerungs-Kunde.  Dresden,  1846, 28  pis. 

Limulus.  Halicyne,  Belinurus,  Eurypterus, 
Cytherina,  Calymene,  Homalonotus,  Dipleura, 
Trimerus,  Cyphaspis,  Phacops,  Aconia,  Illcenus, 
Archegonus,  Asaphus,  Dysplanus,  Nileus,  Am- 
pyx,  Trinucleus,  Ogygia,  Odontopleura,  Arges, 
Bronteus,  Paradoxides,  Olenus,  Conocephalus, 
Ellipsocephalus,  Harpes,  Cytherea,  Cypridina, 
Cyprella,  Cypridella , Pollicipes,  Cyclus. 

Carbonformation  und  Dyas  in  Ne- 
braska. Dresden,  1866,  5 pis. 

Phillipsia  sp.  ?,  Cythere. 

Genzmar.  Beschreibung  einer  ver- 
steinerten  Muschel  mit  dreifachen 
Riicken.  (*) 

In  Gesell.  der  Ober-Lausitz  Lobau,  vol.  2, 
1758;  also,  vol.  3,  p.  185,  fig.  17-21 ; Heues,  Mag., 
Hamburg,  1772. 

This  author  gives  a description  of  the  Trilo 
bites  of  Mecklenburg,  especially  those  of  his 
own  collection. 

Gerstacker  (A.)  In  Bronn’s  Die  Klassen 
und  Ordnungen  der  Arthropoden  wis- 


Gerstacker  (A.)— Continued, 
senschaftlich  dargestellt  in  Wort  und 
Bild.  Crustacea.  Leipzig  und  Heidel- 
berg, 1866-79,  p.  1142,  pis.  43-49. 

Agnostus,  Homalonotus , Phacops,  Dalmani- 
tes,  Cheirurus , Cromus,  Deiphon,  Stauroce-  ' 
phalus,  Ampyx,  Hydrocephalus,  Acidaspis,  Te-  . 
lephus,  JEglina,  Lichas,  Sphcerexochus,  Triar- 
thrus,  Dindymene,  Barrandia,  Illcenus,  Nileus,  \ 
Ogygia.  Bronteus,  Asaphus,  Paradoxides,  Phil - 4 
lipsia,  Carmon,  Ellipsocephalus,  Cyphaspis, 
Arethusina,  Proetus,  Arionellus , Remopjeurides,  | 
Bohemilla,  Calymene,  Conocephalit ^ Olenus, 
Peltura,  Arera,  Sao,  Phacoparia,  Amphion,  * 
Encrinurus,  Zethus.  Trinucleus,  Dionides.  Har-  ■. 
pides,  Harpes,  Aristozoe,  Beyrichia,  Bolbozoe,  [ 
Callizoe,  Caryon,  Crescentilla  Cythere,  Cythe-  jj 
ropsis,  Elpe,  Entomis , Heppa,  Leperditia,  Iso- 
chilina . Orozoe,  Nothozoe,  Primitia,  Zonozoe,  ~ 
Cryptocaris,  Aptychopsis,  Adelophthalmus,  Eu- 
rypterus, Limulus,  Pterygotus,  Belinurus,  Prest- 
wichia,  Hemiaspis. 

Giebel  (C.)  Die  silurische  Fauna  des 
Unterharzes. 

In  Abhandl.  Hat.  Yereins  Sachsen  u.  Thii- 
ringen,  vol.  1, 1858,  p.  1,  7 pis. 

Harpes,  Proetus,  Cyphaspis,  Phacops,  Lichas, 
Dalmannia,  Acidaspis,  Bronteus. 

Goldfuss  (A.)  Observation  sur  la  place 
qu’occupent  les  Trilobites  dans  le  rkgne" 
animal. 

In  Annales  Sci.  Hat.  Paris,  vol.  15, 1828,  p.  83, 
pi.  2. 

Asaphus,  Calymene. 

Catalogue  des  Trilobites. 

In  B andbuch  der  Geognosie  von  de  la  Beche, 
1832. 

This  list  was  copied  by  Dr.  Jacob  Green  in 
his  “Monograph  of  the  Trilobites  of  Horth 
America,”  p.  20. 

Beitrage  zur  Farailie  der  fossilen 

Crustaceen . 

In  Hova  Acta  Physico  Med.,  vol.  19,  1839, 
Breslau,  p.  353,  pi.  33. 

Harpes  n.  g.,  Arges  n.  g.,  Brontes  n.  g.,  II- . 
Icenus?  triacanthus. 

Systematische  Uebersicht  der  Trilo- 

biten  und  Beschreibuug  einiger  neuen 
Arten. 

In  Heues  Jahrbnch  fiir  Mineral.,  1843,  p.  537, 
pis.  4-6. 

Harpes,  Paradoxides , Olenus,  Antlics  n.  g., 
Olenus  scaraboeoides,  Conocephalus,  Ellipsoce* 
phalus , Proetus,  Acaste,  Gerastos  n.  g.,  Phacops , ' 
Calymene,  Homalonotus , Dipleura,  Cryptoli-% 
thus,  Ampyx,  Asaphus,  Isotehis,  Sympliysurus  * 
II.  g.,  Ogygia,  Cryptonymus,  Odontopleura , q 
Ceraurus,  Otarion,  Arges,  Zethus,  Amphion, . 
Bronteus , Illcenus,  Bumastus,  Nileus,  Agnostus. 

Classifies  204  species  under  32  genera. 


V0GDE8.J 


LIST  OF  AUTHORS, 


31 


Goodchild  (J.  G.)  and  Postlethwaite 
(J.).  See  Postlethwaite  (J. ) and 
Goodchild  (J.  G.). 

Green  (Jacob).  Synopsis  of  the  Trilo- 
bites  of  North  America.  In  which  some 
new  genera  and  species  are  proposed. 

Monthly  Am.  Jour.  Geology,  Phila.,  vol.  2, 
1832,  p.  558,  pi.  14.  Republished  in  Dr.  Jacob 
Green’s  “ Monograph  of  the  Trilobites  of  North 
America,’'  Phila.,  1832.  List  given  in  Dr.  R. 
Harlan’s  “Med.  Phys.  Researches,”  Phila., 
1835,  p.  300.  > 

Calymene  blumenbachii , C.  callicephala,  C. 
r selenecephala.  C.  platys,  C.  microps,  C.  ancldops, 

C.  diops,  G.  bufo,  Asaphus  caudatus,  A.  selenu- 
rus,  A.  pleuroplyx,  A.  wetherilli,  A.  micrurus, 
A.  limulurus,  A.  laticostatus,  Tnmerus  n.  g., 
T.  delphinocephalus  (pi.  14,  fig.  1),  Cryptolithus 
n.g.,  G.  tessellatus  (pi.  14,  fig.  4),  Bipleura  n.  g., 

D.  dekayi  (pi.  14,  figs.  8,  9),  Isotelus  gigas,  I 
planus,  I.  cyclops  (pi.  14,  fig.  7),  Triarthrus  n. 
g.,  T.  beckii  (pi.  14,  fig.  6 ),Paradoxides  boltonii 
(pi.  14,  fig.  5),  Ceraurusn.  g.,  0.  pleur exanthe- 
mas (pi.  14,  fig.  10). 

A monograph  of  the  Trilobites  of 

North  America,  with  colored  models  of 
the  species.  Philadelphia,  1832,  94  pp., 

1 pi.  (Oct.  1,  1832). 

Calymene,  Asaphus,  Hemicrup turus  n.  g., 
Ogygia,  Isotelus,  Cryptolithus,  Dipleura,  Tri- 
merus,  Ceraurus,  Triarthrus,  Nuttainia,  Bron- 

gniartia. 

A supplement  to  the  monograph  of 

the  Trilobites  of  North  America,  with 
colored  models  of  the  species.  Phila- 
delphia, 1835,  24  pp.  (May  1,  1835). 
Paradoxides,  Calymene,  Asaphus. 

A new  Trilobite.  Letter  to  the 

editor,  Dec.  26,  1832. 

In  Am.  Jour.  Sci.,  1st  series,  vol.  23,  1833,  p. 
397. 

Asaphus  myrmecoides. 

Description  of  a new  Trilobite  from 

Nova  Scotia. 

In  Trans.  Geol.  Soc.  Pennsylvania,  vol.  1,  pt. 
1, 1834,  p.  37,  pi.  4. 

Asaphus  crypturus. 

Description  of  some  new  North 

American  Trilobites. 

In  Am.  Jour.  Sci.,  1st  series,  vol.  25,  1834,  p. 

334. 

Calymene  odontocephalus,  Asaphus  astragalo- 
tes,  A.'tetragonocephalus,  Paradoxides  harlani' 

Description  of  a new  Trilobite. 

In  Am.  Jour.  Sci.,  1st  series,  vol.  32,  1837,  p. 

167. 

Calymene  phtyctainodes,  Asaphus  platypleu • 

rus. 

■ Description  of  two  new  species  of 

Trilobites.  Read  Jau.  24,  1837. 


Green  (Jacob)— Continued. 

In  Jour.  Acad.  Nat.  Sci.  Phila.,  vol.  7, 1837,  p. 
217,  2 wood-cuts. 

Cryphceus  n,  g.,  C.  boothi,  Asaphus  trimblii. 

J.  W.  Salter  (Mon.  Brit.  Tril.,  p.  15)  gives  the 
following  diagnosis  of  the  genus,  and  uses  it 
as  a subgenus  to  Phacops:  “ Form  of  moderate 
size,  depressed.  Glabella  depressed,  not  much 
expanded  in  front;  all  the  lobes  distinct,  the 
front  ones  not  greatly  enlarged,  genal  angles 
long-spined.  Pleura  truncate,  and  the  hinder 
ones  often  produced  into  spines.  Tail  large,  of 
many  segments;  the  margin  spinose.” 

Description  of  several  new  Trilo- 
bites. 

In  Am.  Jour.  Sci.,  1st  series,  vol.  32, 1837,  p. 
343,  2 wood-cuts. 

Cryphceus,  C.  boothi,  C.  collitelus,  Trimerus 
jacksonii,  Asaphus  trimblii. 

— — Some  remarks  on  the  genus  Para- 
doxides Brong.,  and  the  necessity  of  pre- 
serving the  genus  Triarthrus , proposed 
in  the  Monograph  of  the  Trilobites  of 
North  America. 

In  Am.  Jour.  Sci.,  1st  series,  vol.  33,  1838,  p. 
341. 

Description  of  a new  Trilobite. 

In  Am.  Jour.  Sci.,  1st  series,  vol.  33,  1838,  p. 
406. 

Calymene  rowii. 

This  Trilobite  was  figured  by  Mr.  Row  in  the 
Poughkeepsie  Telegraph,  Nov.  22,  1837. 

Description  of  a new  Trilobite. 

In  Annals  Mag.  Nat.  History,  1st  scries,  vol. 
1, 1838,  p.  79. 

Calymene  rowii. 

The  inferior  surface  of  the  Trilobite 

discovered. 

In  The  Friend,  a weekly  Journal,  Philadel- 
phia, March  16,  1839. 

Calymene  bufo. 

The  inferior  surface  of  the  Trilobite 

discovered.  Illustrated,  with  colored 
models.  Philadelphia,  1839. 

Calymene  bufo. 

Remarks  on  the  Trilobites. 

In  Am.  Jour.  Sci.,  1st  series,  vol.  37,  1839,  p. 
25. 

This  article  appears  to  be  a republicalion  of 
the  two  preceding  references,  with  the  addition 
of  the  remarks  on  p.  38  of  the  Journal 

An  additional  fact,  illustrating  the 

inferior  surface  of  Calymene  bufo. 

In  Am.  Jour.  Sci.,  1st  series,  vol.  38,  1810,  p. 
410. 

Grewingk  (C.)  Geologie  von  Liv-  and- 
Kurland. 

In  Archiv  Natur.  Liv-,  Ehst-  u.  Kurl.,  Dor- 
pat,  vol.  2,  pt.  3,  1861,  p.  571,  4 pis. 

Beyrichia. 


32 


A BIBLIOGRAPHY  OF  PALEOZOIC  CRUSTACEA. 


[BULL.  63. 


Griffith  (Richard). 

Two  important  works  on  the  paleontology 
and  geology  of  Ireland  were  prepared  under 
the  direction  of  Mr.  Richard  Griffith  by  Fred- 
erick McCoy,  who  will  be  counted  as  the 
author,  although  Mr.  Richard  Griffith  was  the 
collector  of  the  specimens  and  the  financial 
supporter  of  the  publications. 

The  contributions  on  the  Paleozoic  Crustacea 
are  given  under  McCoy  (Frederick)  in  this 
work. 

Grote  (A.  R.)  and  Pitt  (W.  H.)  New 
specimen  from  the  Water  Lime  group 
at  Buffalo,  N.  Y. 

In  Proc.  Am.  Assoc.  Adv.  Sci.,  26th  meet- 
ing, Nashville,  1877,  p.  300. 

Pterygotus  cummingsi. 

Description  of  a new  Crustacean 

from  the  Water  Lime  group  at  Buffalo. 

In  Bull.  Buffalo  Soc.  Nat.  Sci.,  vol.  3,  1875, 

p.  1. 

Eusarcus  n.  g. 

On  new  species  of  Eusarcus  and 

Pterygotus  from  the  Water  Lime  group 
at  Buffalo. 

In  Bull.  Buffalo  Soc.  Nat.  Sci.,  vol.  3,  1875,  p. 
17,  plate? 

Eusarcus , Pterygotus. 

Gruenwaldt  (M.)  Beitrage  zur  Kennt- 
niss  der  sedimentaren  Gebirgsforma- 
tionen  des  Ural. 

In  Mem.  Acad.  Sci.  St.-P6tersbourg,  7th  se- 
ries, vol.  2,  No.  7,  1860,  6 pis. 

Phillipsia,  Leperditia. 

Guettard  (E.-T.)  M^moiresur  les  ardoi- 
sibres  d’Angers. 

InM6m.  Acad.  Sci.  Paris,  1757,  p.  52,  pis.  7-9. 
Reprint:  Amsterdam,  1768. 

The  author  in  his  memoir  on  the  geology  of 
Angers  gives  descriptions  and  figures  of  several 
Trilobites.  These  were  afterwards  described 
by  Alex.  Brongniart  under  the  genus  Ogygia 
and  named  by  this  author  Ogygie  de  Guettard 
and  O.  desmarestii. 

Haldeman  ( S.  S. ) On  the  supposed  iden- 
tity of  Atops  trilineaius  with  Triarthrus 
becJcii. 

In  Am.  Jour.  Sci.,  2d  series,  vol.  5,  1848,  p. 
107. 

Hall  (Charles  E.)  Contribution  to  palae- 
ontogy  from  the  Museum  of  the  Second 
Geological  Survey  of  Pennsylvania. 

In  Proc.  Am.  Philos.  Soc.,  Phila.,  vol.  16, 1877, 

p.  621. 

Eurypterus. 

Hall  (James).  Description  of  two  species 
of  Trilobites  belonging  to  the  genus 
Paradoxides. 


Hall  (James) — Continued. 

In  Am.  Jour.  Sci.,  1st  series,  vol.  33,  1838,  p. 
139,  2 figs. 

Read  before  th e T ale  N at ural  History  Society, 
March  21, 1837. 

Paradoxides  beckii , P.  eatoni. 

Trilobites  of  the  inferior  strata. 

(Extracted  and  published  in  advance  of  the 
“Palaeontology  of  New  York,”  vol.  1,  Albany, 
1846,  p.  225,  pis.  60-67.) 

Olenus,  Phacops,  Calymene,  Platynotus,  Tri- 
nucleus, Asaphus  Isotelus,  Acidaspis,  Ceraurus , 
lllcenus , Agnostus. 

Palaeontology  of  New  York.  Yol.  1. 

Containing  descriptions  of  the  organic 
remains  of  the  lower  divisions  of  the 
New  York  system.  Albany,  1847,  LOO 
pis. 

Olenus , Phacops , Calymene,  Platynotus , Tri- 
nucleus, Asaphus , Isotelus,  Acidaspis,  Cerau- 
rus, lllcenus,  Agnostus. 

Remarks  on  the  observations  of  S. 

S.  Haldeman  “ On  the  supposed  iden- 
tity of  Atops  trilineatus  with  Triarthrus 
beckii.” 

In  Am.  Jour.  Sci.,  2d  series,  vol.  5, 1848,  p.  322, 
10  wood-cuts. 

Descriptions  of  new  species  of  fos- 
sils, and  observations  upon  some  others 
previously  not  well  known,  from  the 
Trenton  limestones. 

In  Third  Rept.  New  York  State  Cab.  Nat. 
Hist.,  1850,  p.  167,  5 pis.  (2  eds.). 

Asaphus  extans. 

This  species  was  used  by  Mr.  E.  Billings  for 
the  type  of  Bathyurus. 

Description  of  new  or  rare  species  of 

fossils  from  the  Palaeozoic  series. 

In  Rept.  Geol.  Lake  Superior  Land  Dist. 
(Foster  and  Whitney),  1851,  pt.  2,  p.  203,  pis. 
22-35. 

Harpes  escanabice,  Dikelocephalus , Proetus, 
Phacops  anchiops,  P.  callicephalus,  Asaphus 
barrandi-,  tracks  of  a Crustacean  ? 

Palaeontology  of  New  York.  Yol.  2. 

Containing  descriptions  of  the  organic 
remains  of  the  lower  divisions  of  the 
New  York  system.  Albany,  1852,  104 
pis. 

Phacops,  Proetus,  Calymene,  Homalonotus, 
Arges,  Lichas,  Acidaspis,  Ceraurus,  Cybele, 
Bumastis,  Beyrichia,  Cytherina,  Onchus. 

Noies  on  some  fossils  of  the  so-called 

Taconic  system  described  by  Doctor 
Emmons. 

In  Am.  Jour.  Sci.,  2d  series,  vol.  19,  1855,  p. 
434. 

Olenus  ( Ell^ptocephalus ) asaphoides. 


VOGDES.] 


LIST  OF  AUTHORS, 


33 


Hall  (James) — Continued. 

Description  of  new  species  of  fossils 

from  the  Carboniferous  limestone  of  In- 
diana and  Illinois. 

Read  in  1856  and  published  separately  by  the 
author.  See,  also,  Trans.  Albany  Inst.,  vol.  I, 
pt.  1, 1857,  p.  1. 

Cytherina  carbonaria. 

Descriptions  of  these  fossils,  with  additional 
notes  by  R.  P.  Whitfield,  were  published  in  the 
Bull.  Am.  Mus.  Nat.  Hist.,  New  York,  vol.  1,  No. 
3,  1882. 

The  original  descriptions,  with  additional  ob- 
servation by  James  Hall,  with  the  plates  from 
R.  P.  Whitfield’s  memoir,  were  published  in  the 
12th  Annual  Rept.  Geol.  Nat.  Hist.  Indiana, 
1882,  pp.  321-375,  pis.  29-32. 

The  Trilobites  of  the  shales  of  the 

Hudson  River  group. 

In  Twelfth  Rept.  New  York  State  Cab.  Nat. 
Hist.,  1859,  p.  59,  3 wood-cuts.  See,  also,  Pa- 
laeont.  New  York,  vol.  3,  1859;  Geol.  Vermont, 
vol.  1,  1861 ; 13th  Rept.  New  York  State  Cab. 
Nat.  Hist.,  1860. 

Olenus  thornp8oni,  O.  vermontana,  Peltura 
( Olenus ) holopyge. 

Geological  Survey  New  York.  Palae- 
ontology. Yol.  3.  Containing  descrip- 

' tions  and  figures  of  the  organic  remains 
of  the  Lower  Helderberg  group  and  the 
Oriskany  sandstone.  1855-’59. 

Pt.  1,  text,  1859;  pt.  2,  plates,  1861, 120  pis. 

Proetus,  Phacops,  Dalmania,  Homalonotus, 
Licha8,  Acidaspis , Bronteus,  Eurypterus,  Doli- 
chopterus  n.  subgenus,  Pterygotus,  Leperditia , 
Beyrichia,  Ceratiocaris,  Olenus  thompsoni,  O. 
vermontana,  Peltura  {Olenus)  holopyge. 

Description  of  new  species  of  fossils 

from  the  Silurian  rocks  of  Nova  Scotia. 

In  Canadian  Naturalist,  vol.  5, 1860,  p.  144. 

Homalonotus  dawsoni  Hall,  Calymene  blu- 
menbachii , Dalmania  logani  Hall,  Beyrichia 
pustulosa  Hall,  B.  ceqilatera  Hall,  Leperditia 
sinuata  Hall. 

Contributions  to  palaeontology,  1858 

and  1859.  Notes  and  observations  upon 
the  fossils  of  the  Goniatite  limestone  in 
the  Marcellus  shale  of  the  Hamilton 
group  in  the  eastern  and  central  parts 
of  the  State  of  New  York,  and  those  of 
the  Goniatite  beds  of  Rockford,  In- 
diana ; with  some  analogous  forms  from 
the  Hamilton  group  proper. 

In  Thirteenth  Rept.  New  York  State  Cab. 
Nat.  Hist.,  1S60,  p.  95. 

Proetus  doris  Hall. 

Note  upon  the  Trilobites  of  the  shales 

of  the  Quebec  group  in  the  town  of 
Georgia,  Vermont. 

Bull.  63 3 


Hall  (James) — Continued. 

In  Thirteenth  Rept.  New  York  State  Cab. 
Nat.  Hist.,  I860,  p.  113. 

Barrandia  n.  g. 

This  term  was  used  by  Frederick  McCoy, 
in  1844,  for  a genus  of  Trilobites. 

Bathynotus  n.  g. 

New  species  of  fossils  from  the  Hud- 
son River  group  of  Ohio  and  the  West- 
ern States. 

In  Thirteenth  Rept.  New  York  State  Cab. 
Nat.  Hist.,  1860,  p.  119. 

Oalymene  christyi,  Proetus  parviusculus. 

Geological  Survey  of  Wisconsin. 

Description  of  new  species  of  fossils 
from  the  investigations  of  the  survey, 
etc.  Report  of  the  superintendent  of 
the  Geological  Survey,  exhibiting  the 
progress  of  the  work,  January  1,  1861, 

p.  11. 

Dalmanites , Oalymene,  lllcenus. 

Preliminary  notice  of  the  Trilobites 

and  other  Crustacea  of  the  Upper 
Helderberg,  Hamilton,  and  Chemung 
groups. 

Author’s  edition,  published  in  1861,  11  pis., 
170  pp. ; 15th  Rept.  New  York  State  Cab.  Nat. 
Hist.,  1862,  p.  82. 

Olenellus  n.  g.,  Proetus,  Phacops,  Dalmania , 
Calymene,  Homalonotus,  Lichas,  Acidaspis , 
Beyrichia,  Leperditia. 

Note  on  the  genus  Cypricardites. 

In  Fifteenth  Rept.  New  York  State  Cab.  Nat. 
Hist.,  1861,  p.  192.  Plate  illustrating  certain 
genera  and  species  described  by  T.  A.  Conrad 
in  the  5th  Annual  Rept.  Pal.  Dept.  New  York 
Geol.  Survey,  1841,  pi.  11  (reprint). 

Dicranurus,  pi.  11,  fig.  1;  Aspidolites,  pi.  11, 
fig.  2 ; Acidaspis  tuberculatus,  pi.  11,  fig.  3. 

Note  upon  the  Trilobites  of  the  Hud- 
son River  group,  in  the  town  of  Georgia, 
Vermont. 

In  Geol.  Vermont,  vol.  1,  1861,  p.  367,  pi.  13. 

Barrandia,  B.  vermontana,  Bathynotus,  B. 
holopyga. 

Palaeontology  of  Wisconsin.  Re- 
marks upon  the  condition  of  the  fossils 
in  the  rocks  of  the  several  formations. 
Catalogue  of  fossils  known  in  the  Palae- 
ozoic formations  of  Wisconsin,  with 
observations  upon  some  of  the  known 
species  and  descriptions  of  several  new 
forms. 

Geol.  Survey  Wisconsin,  vol.  1,  1862,  p.  425. 

On  a new  Crustacean  from  the  Pots- 
dam sandstone.  A letter  addressed  to 
Principal  Dawson,  dated  Albany,  Oct. 
31,  1862. 


34 


A BIBLIOGRAPHY  OF  PALEOZOIC  CRUSTACEA. 


I BULL.  63. 


Hall  (James) — Continued. 

In  Canadian  Naturalist,  vol.  7,  1862,  p.  443, 
figure.  See  The  Geologist,  vol.  6,  London,  1863, 
p.  247,  figure. 

Aglaspis  n.  g. 

On  the  occurrence  of  Crustacean  re- 
mains of  the  genera  Ceratiocaris  and 
Dithyrocaris , with  a notice  of  some  new 
species  from  the  Hamilton  group  and 
Genesee  slate. 

In  Sixteenth  Kept.  New  York  State  Cab.  Nat. 
Hist.,  Albany,  1863,  p.  71,  plate. 

Preliminary  notice  of  the  fauna  of 

the  Potsdam  sandstone,  with  remarks 
upon  the  previously  known  species  of 
fossils,  aud  description  of  some  new 
ones  from  the  sandstones  of  the  Upper 
Mississippi  Valley. 

In  Sixteenth  Kept.  New  York  State  Cab.  Nat. 
Hist.,  1863,  p.  119,  6 pis.  Supplementary  note, 

p.  110. 

Dikelocephalus,  Triarthrella  n.  g.,  Conocepha- 
lus , Arionellus,  Chariocephalus  n.  g.,  Ptychas- 
pis  n.  g.,  Lichas,  lllcenurus  n.  g.,  AmpMon?, 
Agntfstus,  Pemphigaspis  n.  g.,  Aglaspis. 

Notice  of  some  new  species  of  fossils 

from  a locality  of  the  Niagara  group  in 
Indiana,  with  a list  of  identified  spe- 
cies from  the  same  place. 

In  Trans.  Albany  Inst.,  vol.  4,  1864,  p.  195. 
Author’s  edition  published  May  2, 1863,  pp.  1-34. 

Dalmania,  Cyphaspis,  Lichas. 

Plates  of  the  species.  28th  Kept.  New  York 
State  Mus.  Nat  Hist.,  1879. 

Account  of  some  new  or  little  known 

species  of  fossils  from  rocks  of  the  age 
of  the  Niagara  group. 

In  T wen  t ietb  Kept.  N ew  Y ork  State  C ab.  N at. 
Hist.,  1867,  p.  305,  21  pis.  Originally  printed 
in  advance  for  the  18th  Keport  New  York  State 
Cab.  Nat.  Hist.,  1864.  Kevised  edition,  Albany, 
1870,  with  22  pis. 

Dalmania , Calymene,  Lichas , Acidaspis, 
Ceraurus , Sphcerexochus,  lllcenus,  Encrinurus, 
Bronteus. 

Geological  Survey  of  the  State  of 

Wisconsin,  ISfiiMfiS.  Palaeontology. 
Pt.  3.  Organic  remains  of  the  Niagara 
group  and  the  associated  limestones. 
94  pp.,  18  pis.  Albany,  1871. 

The  same  was  published  in  1864  in  advance 
for  tbe  18th  Rept.  New  York  State  Cab.  Nat. 
Hist.,  1867,  under  tbe  title  of  “Account  of  some 
new  or  little  known  species  of  fossils  from  rocks 
of  the  ago  of  the  Niagara  group.”  See  20th 
Kept.  New  York  State  Cab.  Nat.  Hist.,  rev. 
edition,  1870,  p.  347. 


Hall  (James) — Continued. 

Descriptions  of  new  species  of  fossils 

from  the  Hudson  River  group  in  the 
vicinity  of  Cincinnati,  Ohio. 

In  Twenty-fourth  Rept.  New  York  State  ' 
Mus.  Nat.  Hist.,  Albany,  1872,  p.  225,  1 pi. 

Published  Oct.,  1871,  in  advance  of  the  State  , 
Cab.  report. 

Leperditia,  Beyrichia. 

Descriptions  of  new  species  of  Cri- 

noids  and  other  fossils  from  strata  of 
the  age  of  the  Hudson  River  group  and 
Trenton  limestone. 

In  Twenty -fourth  Rept.  New  York  State 
Mus.  Nat.  Hist.,  1872,  p.  205,  3 pis. 

Dalmania  breviceps,  Proetus  parviusculus. 

Advance  sheets  of  this  article  were  printed  i 
and  distributed  in  November,  1866,  except  the 
first  four  species  of  Crinoidea  mentioned  in  the 
foot-note  on  p.  205,  which  were  first  published 
in  1871  in  a pamphlet  entitled  “ New  species  of 
fossils  from  the  Hudson  River  group  in  the  I 
vicinity  of  Cincinnati,  Ohio.” 

The  fauna  of  the  Niagara  group  in 

central  Indiana. 

Documents  only  of  Twenty-eighth  Rept. 
New  York  State  Mus.  Nat.  Hist.,  1876,  34  pis.  "! 

The  fauna  of  the  Niagara  in  central 

Indiana. 

In  Twenty-eighth  Rept.  New  York  State 
Mus.  Nat.  Hist.,  1879,  p.  99,  34  pis. 

Cyphaspis , Dalmanites,  Odontocephalus,  Caly-~- 
mene,  Homalonotus,  Lichas , Ceraurus,  lllcenus , 1 
Beyrichia , Leperditia. 

Illustrations  of  Devonian  fossils : 

Gasteropoda,  Pteropoda,  Cephalopoda, 
Crustacea,  and  Corals  of  the  Upper 
Helderberg,  Hamilton,  and  Chemung 
groups,  etc.  Albany,  1876, 7 pp. , 133  pis. 

Proetus , Phillipsia  (Brachymetopus  ?),  Pha- 
cops,  Dalmanites,  Calymene,  Homalonotus,  Li - ] 
chas,  Acidaspis  ( Terataspis ),  Dithyrocaris , Cera-  I 
tiocaris. 

Descriptions  of  new  species  of  fossils  | 

from  the  Niagara  formation  at  Waldron, 
Indiana. 

In  Trans.  Albany  Inst.,  vol.  10,  1883,  p.  57.  I 
Read  1879,  and  published  separately  in  1881.  * 

Acidaspis  fimbriata , lllcenus  ( Bumastus ),  1 
Ioxus. 

Description  of  the  species  of  fossils  (1 

found  in  the  Niagara  group  at  Waldron, 
Indiana. 

In  Eleventh  Ann.  Rept.  for  1881,  Dept.  Geol.  | 
Nat.  Hist.  Survey  Indiana,  1882,  p.  217,  36  pis.  I 

Cyphaspis,  Dalmanites,  Odontocephalus.  Caly • N 
mene,  Homalonotus,  Lichas,  Acidaspis,  lllcenus , k 
I Beyrichia,  Leperditia. 


VOGDES.] 


LIST  OF  AUTHORS. 


Hall  (James) — Continued. 

Note  on  the  Eurypteridce  of  the  De- 
vonian and  Carboniferous  formations 
of  Pennsylvania,  with  a supplementary 
note  on  the  Stylonurus  excelsior. 

In  Proc.  Ain.  Assoc.  Adv.  Sci.,  33d  meeting, 
Phila.,  1884,  p.  420. 

Eurypteridce  from  the  Devonian  and 

Carboniferous  formations  of  Pennsyl- 
vania. With  6 pis. 

Extracted  Kept.  Prog.  PPP.,  2d  Geol.  Survey 
Pennsylvania,  1884. 

Note  on  the  Eurypteridce  of  the  De- 
vonian and  Carboniferous  formations 
of  Pennsylvania. 

In  Second  Geol.  Survey  Pennsylvania,  Eept. 
Prog.  PPP.,  1884,  6 pis. 

Eurypterus,  Dolichopterus,  Pterygotus,  Stylo- 
nurus, Eurypterus  (Anthraconectes)  mazonensis 

M.  & W. 

Description  of  a new  species  of 

Stylonurus  from  the  Catskill  group. 

In  Thirty-sixth  Eept.  New  York  State  Mus. 
Nat.  Hist.,  1884,  p.  76,  pi.  5. 

Stylonurus  excelsior  Hall. 

There  was  a short  notice  of  this  species  pub- 
lished by  D.  S.  Martin  (Trans.  New  York 
Acad.  Sci.,  vol.  2,  1882,  p.  8).  This  notice  was 
based  upon  a cast  of  the  carapace  in  the  New 
York  State  Museum,  which  had  been  labeled 
with  name  and  locality  by  Prof.  James  Hall. 

and  Whitfield  (R.  P.)  Descriptions 

of  new  species  of  fossils  from  the  vi- 
cinity of  Louisville,  Ky.,  and  the  Falls 
of  the  Ohio. 

In  Twenty-fourth  Eept.  New  York  State 
Mus.  Nat.  Hist.,  1872,  p.  181,  pi.  13,  figs  20  and 21. 

Illcenus  cornigerus  H.  & W. 

Geological  Survey  of  Ohio. 

Vol.  2.  Geology  and  palamntology. 
Pt.  2.  Palaeontology.  1875,  p.  67,  pis. 

1-12. 

Proetus,  Dalmania , Galymene,  Lichas,  Encri- 
nurus,  Leperditia  ( Isochilina ),  Beyrichia,  Plu- 
mulites. 

Palaeontology. 

In  U.  S.  Geol.  Expl.  40th  Parallel,  vol.  4,  pt. 
2, 1877,  7 pis. 

Dikellocephalus,  Conocephalites,  Crepicepha- 
lus  ( LoganeUus ),  Ptychaspis , Ghariocephalus, 
Bathyurus,  Proetus,  Ogygia,  Agnostus. 

•  and  Clarke  (John  M.)  Geological 

• Survey  of  the  State  of  New  York. 
Palaeontology.  Vol.  VII.  Text  and. 
plates,  containing  descriptions  of  the 
Trilobites  and  other  Crustacea  of  the 
Oriskany,  Upper  Helderberg,  Hamil- 
ton, Portage,  Chemung,  and  Catskill 
groups.  Albany,  1888,  236  pp.,  36  pis. 


35 

Hall  (James)  and  Clarke  (John  M.) — 
Continued. 

Trilobita : Galymene , Homalonotus,  Bron- 
teus,  Phacops,  Dalmanites  subgen.,  Haus- 
manni  n.  s.  g.,  Coronura  n.  s.  g.,  Cryphceus. 
Odontocephalus,  Gorycephalus,  Ghasmops,  Li- 
chas subgen.,  Terataspis,  Gonolichas . Hoplo- 
chas , Arges , Geratolichas,  Proetus , Phcethonides, 
Gyphaspis. 

Xiphosura:  Protolemulus,  Eurypterus , Stylo- 
nurus. 

Phyllocoridfe : Ceratiocaris,  Echinocaris,  Ely- 
mocaris,  Tropidocaris. 

Pinsecaridae : Mesothyra  n.  g. 

Ehinocardse:  Bhinocaris  n.  g. 

Discinocaridse : Spathiocaris,  Dipterocaris. 

Decapoda : Palceopalcemon. 

Phyllopoda : Estheria,  Schizodiscus  n.  g. 

Cirripidae : Protobalanus. 

Palseocreusia : Stropbilepis  n.  g.,  Turrilepas. 

Hancock  ( Abbany).  Remarks  on  certain 
vermiform  fossils  found  in  the  mountain 
limestone  districts  of  the  north  of  Eng- 
land. 

In  Eept.  28th  Meeting  Brit.  Assoc.  Adv.  Sci., 
1858,  Tran,  of  Sec.,  p.  80. 

Tracks  of  Trilobites. 

Harlan  (Richard).  Critical  notices  of 
various  organic  remains  hitherto  dis- 
covered in  North  America. 

In  Trans.  Geol.  Soc.  Pennsylvania,  vol.  1,  pt. 

1. 1834,  p.  46,  1 pi. 

The  author  herein  describes  two  species  of 
Eurypterus  and  gives  a list  of  North  American 
Trilobites. 

Eurypterus  remipes  lie  Kay,  E.  lacustris 
Harlan. 

Notice  of  nondescript  Trilobites  from 

the  State  of  New  York,  with  observa- 
tions on  the  genus  Triarthrus,  etc. 

In  Trans.  Geol.  Soc.  Pennsylvania,  vol  1,  pt. 

2. 1835,  p.  263,  pi.  15. 

Paradoxides  triarthrus  Har.,  P.  arcuatus 
Har.,P.  scaraboides  Brong. 

Medical  and  physical  researches,  or 

original  memoirs  in  medicine,  surgery, 
physiology,  geology,  zoology,  etc. 
Phila.,  1835,  36  pis. 

Contains  a republication  of  the  above  articles 
under  Harlan,  pp.  253-313  and  400-403. 

Hartt  (C.  F.)  Fossils  of  the  Primordial 
or  Acadian  group  at  St.  John. 

In  Acadian  Geology,  the  geological  struct- 
ure, organic  remains,  and  mineral  resources  of 
Nova  Scotia,  etc.,  by  J.  W.  Dawson,  2d  ed., 
London,  1868,  pp.  641-657;  also  3d  ed.,  1 878, 
with  supplement  (wood-cuts). 

Paradoxides,  Gonocepliahtes,  Microdiscus,  Ag- 
nostus. 

Mr.  ('.  F.  nartt,  in  his  original  description  of 
Microdiscus  dawsoni  Hartt,  described  the  spe- 
cies under  the  new  generic  name  of  Dawsonia. 


36  A BIBLIOGRAPHY  OF  PALEOZOIC  CRUSTACEA.  {bull.  63. 


Hartt  (C.  F.) — Continued. 

In  the  Acadian  Geology  the  species  is  placed 
under  the  genus  Microdiscus  on  the  authority 
of  Mr.  E.  Billings,  of  the  Canadian  Geological 
Survey. 

Appendix  B.  List  of  New  Bruns- 
wick fossils. 

See  Bailey’s  “Observations  on  the  Geol.  of 
Southern  New  Brunswick,  etc.,”  1865,  p.  143.  j 

and  Rathbun  (Rickard).  Morgan 

Expedition,  1870-  71.  On  the  Devonian 
Trilobites  and  Mollnsks  of  Erer6,  Prov-  j 
ince  of  Pard.,  Brazil. 

In  AnDals  Lyceum  Nat.  Hist.,  New  York, 
vol.  11,  1875,  p.  110. 

Dalmania  paituna  H.  & R.,  Homalonotus 
oiara  H.  & R. 


Herrick  (C.  L.)— Continued. 

Appendix  2.  A Waverly  Trilobite. 

In  Bull.  Denison  Univ.,  vol.  2,  pt.  1, 1887,  p.  69, 
pi.  7,  fig.  14. 

Phillipsia  shumardi  Herrick. 

The  geology  of  Licking  County, 

Ohio.  Pt.  IY.  The  Subcarboniferous 
and  Waverly  groups. 

In  Bull.  Denison  Univ.,  vol.  3, 1888,  p.  13,  pis. 
2,  11,  and  12. 

Phillipsia  meramecensis  Sh.,  P.  shumardi 
Her.,  P.  precursor  Her. 

On  the  Trilobites  of  the  Ohio  Wa- 
verly group. 

In  Author’s  advance  sheets  from  the  Bull. 
Denison  Univ.,  vol.  4,  1889,  1 pi. 

Proetus,  Phcethonides,  Phillipsia,  Cythere. 


Hauer  (F.  von).  Ueber  Barrande’s  Ver-  I 
such  einer  Classifikation  der  Trilobiten. 

In  Sitzungsber.  d.  Wien.  Akad.  Math.-na- 
turw,  Classe,  Y,  p.  304,  1850. 

Haulp  (K.)  Die  Fauna  der  Graptkoli- 
tengest. 

In  Lausitzische  Mag.,  vol.  44,  Gorlitz,  1878,  p. 
75,  pi.  5. 

Beynchia. 

Hawle  (Ignaz).  See  Corda  (A.  J.  C.) 
and  Hawle  (Ignaz). 

Hayden  (F.  V.)  See  Meek  (F.  B.)  and 
Hayden  (F.  V.). 

Heidenkain  (F.)  Ueber  Graptholiten-  | 
fiikrende  Diluvial-Geschiebe  der  nord-  j 
deutschen  Ebene. 

In  Zeitschr.  Deutsch.  geol.  GeselL,  vol.  21, 
1869,  p.  143,  plate. 

Calymene  blumenbachi,  Dalmanites  caudata, 
Odontopleura  ovata,  O.  nutica,  Cyphaspis, 
Homalonotus,  Beyrichiakloeden,  B.  maccoyana, 
B.  tuber culatus. 

Heilman  (A.)  Die  Petrefacten  Thiirin- 
gens.  Cassel,  1866,  5 pts.,  24  pis. 

Dalmania  tuberculata,  Acidaspis  buchi,  Para- 
doxides  spinosus. 

Hermann  (L.  D.)  Maslographia  Brig®, 
Massel,  1711,  pi.  9,  fig.  50;  pi.  11,  fig.  j 
44;  pi.  12,  fig.  31. 

The  author  herein  compares  a fragment  of 
the  pygidium  of  an  Encrinurus  to  a scollop 
shell. 

Herrick  (C.  L.)  A sketch  of  the  geolog- 
ical history  of  Licking  County,  accom- 
panying an  illustrated  catalogue  of 
Carboniferous  fossils  from  Flint  Ridge, 
Ohio. 

In  Bull.  Denison  Univ.,  vol.  2,  pt.  1,  1887,  p. 

5,  7 pis. 

Proetus,  Phillipsia,  GriJ/ithides,  Brachyme- 
topus,  Dalmanites  ?. 


Notes  upon  the  Waverly  group  in 

Ohio. 

In  Am.  Geologist,  vol.  3, 1889,  p.  94,  4 pis.  (not 
descriptive). 

Hibbert  (Dr.)  On  the  fresh-water  lime- 
stone of  Burdiehouse,  in  the  neighbor- 
hood of  Edinburgh,  belonging  to  the 
Carboniferous  group  of  rocks;  with  sup- 
plementary notes  on  other  fresh-water 
limestones. 

In  Trans.  Royal  Soc.  Edinburgh,  vol.  13, 1836, 
p.  169,  pi.  9. 

The  author  gives  reduced  figures  of  Euryp - 
terus  remipes  De  Kay  and  E.  lacustris  Harlan, 
taken  from  Dr.  Richard  Harlan’s  article  on 
“Organic  Remains  of  North  America.” 

Hicks  ( Henry ).  Note  on  the  genus 
Anopolenus. 

In  Quart.  Jour.  Geol.  Soc.  London,  vol.  21, 
1865,  p.  477,  figures. 

Anopolenus. 

Description  of  new  species  of  fos- 
sils from  the  Longmynd  rocks  of  St. 
David’s. 

In  Quart.  Jour.  Geol.  Soc.  London,  vol.  27, 

1871,  p.  399,  pi.  15. 

Paradoxides,  Plutonia,  Conocoryphe,  Micro- 
discus, Agnostus,  Leper ditia?. 

On  some  undescribed  fossils  from  the 

Menevian  group,  with  a note  on  the  En- 
tomostraca  by  Prof.  T.  Rupert  Jones. 

In  Quart.  Jour.  Geol.  Soc.  London,  vol.  28, 

1872,  p.  173,  pis.  5-7. 

Anoplenus,  Cerausia  n g.,  Erinnys , Cono- 
coryphe, Arionellus , Holocephalina,  Agnostus, 
Leperditia,  Entomis. 

On  the  Tremadoc  rocks  in  the  neigh- 
borhood of  St.  David’s,  South  Wales, 
and  their  fossil  contents. 

In  Quart.  Jour.  Geol.  Soc.  London,  vol.  29, 

1873,  p.  39,  3 pis. 

Neseurctus  n.  g.,  Niobe. 


VOGDES.J 


LIST  OF  AUTHORS. 


37 


Hicks  (Henry) — Continued. 

Descriptions  of  new  species  of  fos- 
sils from  the  Arenig  group  of  St. 
David’s. 

In  Quart.  Jour.  Geol.  Soc.  London,  vol.  31, 

1875,  p.  182,  3 pis. 

Phacops,  Galymene,  Trinucleus,  Ampyx,  Bar- 
randia,  JEglina,  Placoparia,  Illcenus , 1 llcenop- 
sis?. 

Appendix  to  Fossiliferous  Cambrian 

shales,  near  Caernarvon,  by  J.  E.  Marr. 

In  Quart.  Jour.  Geol.  Soc.  London,  vol.  32, 

1876,  p.  135. 

Caryocaris,  JEglina . 

Hisinger  (W.)  Anteckningar  i physik 
och  geognosi  under  resor  uti  Sverige 
och  Norrige.  Stockholm,  8 pts.,  1828- 
’40. 

The  first  three  parts  contain  scarcely  any- 
thing on  Crustacea;  the  remaining  parts  con- 
tain only  enumerations  of  fossils,  without  de- 
scriptions. 

Cytherina  phaseolus  His.,  pt.  5,  pi.  8,  fig.  3. 

* Tableau  des  purifications  de  la 

Suede  distributes  en  ordre  systtma- 
tique.  Stockholm,  1829. 

This  work  enumerates  40  species  of  Silurian 
Crustacea  previously  described  by  J.  W.  Dal- 
man. 

The  second  edition  of  this  work  bears  the 
title  “Esquisse  d’un  tableau  des  petrifications 
de  la  SuMe,”  Stockholm,  1831. 

This  work  contains  43  pages  and  a syste- 
matic table  of  the  fossils,  in  which  46  species 
of  fossil  Crustacea  are  mentioned. 

Lethaea  Svecica,  seu  petrificata  Sve- 
ciae iconibus  et  characteribus  illustrata 
duobus  supplements.  Holmiae,  1837- 
’41,  4to,  42  pis. 

The  first  part  of  this  work  was  published  in 
1835  under  the  title  “leones  petrifica'orum 
Sveciae.  Fas.  I.  Aniraalia  articulata  et  mollusca 
Cephalopoda.”  The  plates,  1 to  10,  were  sent 
by  the  author  only  to  his  friends.  In  1837, 
Lethaea  Svecica  was  published;  it  contained 
124  pages  and  39  plates.  The  first  three  are 
marked  A,  B,  C.  The  fossil  Crustacea  de- 
scribed in  this  work  are  those  of  J.  W.  Dal- 
man’s  Palieaderna,  with  copies  of  his  descrip- 
tions and  figures.  The  second  supplement, 
pxtblished  at  Stockholm  in  1840,  contains  eleven 
pages  and  three  plates.  Figures  and  descrip- 
tions of  Galymene  clavifrons,  Asaphus  ( Tri- 
nucleus) secticorni8,  A.  cyllarus  (Trinucleus) 
and  Galymene  (Gheirurus)  speciosa.  “Lethaea 
Svecica,  seu  petriiicata  Sveciae,  supplementa 
secundi  continuatio,’’  was  published  at  Stock- 
holm in  1841;  it  contains  six  pages  and  three 
plates  (60-62).  Figures  and  description  of  a 
Galymene. 


Hoeninghaus  ( F.  W.  ) Besckreibung 
iiber  Abbildungen  von  Calymene  aracli - 
noides.  Crefeld,  1835,  1 pi.  '(*) 

Ueber  die  Yersteinerungen  des 

Uebergangs-Tkonsckiefers  von  Weis- 
senback  im  Dillenburgscken.  (*) 

In  Isis  (oder  Encycl.  Zeitung),  Oken,  1830,  p. 
96  ; Nones  Jahrbuch  fur  Mineral.,  1831,  p.  341. 

Galymene  macrophthalma. 

Trilobiten  der  geognostiseken 

Sammlung.  Crefeld,  1843,  plate.  * (*) 

Asaphus  dalmani. 

Harpes  reflexus.  Crefeld,  1847,  1 p., 

lpl. 

Hoffman  (E.)  Sammtlicke  bis  jetzt  be- 
kannte  Trilobiten  Russlands. 

In  Verhandl.  russ.  k.  mineral.  Gesell.  zu  St. 
Petersburg,  1857-’58,  p.  21,  7 pis. 

Proetus,  Phillipsia,  Phacops , Ghasmops , 
Galymene , Lichas,  Ampyx , Asaphus , Gheirurus , 
Sphcerexockus,  Zetlius , Encrinurus,  Amphion , 
Bronteus,  Illcenus , Nileus,  Agnostus. 

Holl  (F.)  Handbuch  der  Petrefacten- 
kunde,  etc.  Dresden,  1841,  p.  155. 

Galymene , Asaphus,  Nileus,  Illcenus,  Lichas , 
Ampyx,  Ogygia,  Olenus,  Batlus. 

The  author  gives  short  descriptions  of  the 
Trilobites  described  by  Alex.  Brongniart,  J. 
W.  Dalman,  E.  Eichwald,  von  Schlotheim, 
and  others. 

Holl  (H.  B.)  See  Jones  (T.  Rupert)  and 
Holl  (H.  B.). 

Hollier  (E.)  On  a specimen  of  Homalo- 
notus  delphinocephalus  found  at  Dudley. 

Trans.  Manchester  Geol.  Soc.,  vol.  S,  1869, 

p.  28. 

Holm  ( Gerkard  ) . Anteckningar  om 
Waklenberg’s  Illcenus  crassicauda. 

In  Svenska  Vetensk.  Akad.  Forhandl.,  1880, 
No.  4,  p.  3,  Stockholm,  pi.  5. 

Bemerk ungen  iiber  Illcenus  crassi- 
cauda Wakl. 

In  Zeitschr.  deutscli.  geol.  Gesell.,  vol.  32,  pt. 
2-4,  1880,  p.  559,  pi.  23. 

Ueber  einige  Trilobiten  aus  dem 

Pkyllograptus-Sckiefer  Dalekarliens. 

In  Kongl.  Svenska  Vet.  Akad.  Handl.,vol.  6, 
No.  9, 1882,  pi.  5. 

Pliomera  tornquisti,  Megalaspis  dalecarlicus, 
Ampyx  pater,  Agnostus  tornquisti,  Trilobites 
brevifrons. 

De  Svenska  arterna  af  Trilobitolag 

tet  Illcenus  Dalman. 

In  Kongl.  Svenska  Vet.  Akad.  nandl., vol.  7, 
No.  3,  1882,  6 pis. 


38 


A BIBLIOGRAPHY  OF  PALEOZOIC  CRUSTACEA. 


[BUL£.  63. 


Holm  (Gerhard)— Continued. 

Om  thoraxledernas  antal  lios  Para- 

doxides  tessini  Brongn. 

In  Geol.  Foreningens  Stockholm  Forhandl., 
vol.  9, 1887,  p.  408. 

Om  forekomsten  af  en  Cruziana  i 

ofversta  Olenidskiffern  vid  Knifvinge  i 
Vreta  Kloster  Socken  i Ostergotland. 

In  Geol.  Foreningens  Stockholm  Forhandl., 
vol.  9, 1887,  p.  412. 

Om  Olenellus  kjerulfi  Linrs. 

In  Geol.  Foreningens  Stockholm  Forhandl., 
vol.  9, 1887,  p.  493,  pis.  14, 15. 

Honeyman  (D.)  On  new  localities  of 
fossiliferous  Silurian  rocks  in  e’astern 
Nova  Scotia. 

In  Canadian  Naturalist,  vol.  5,  1860,  p.  293. 

Dr.  J.  W.  Dawson  adds  a note  to  this  paper, 
describing  Homalonotus  dawsoni  Hall,  fig.  1, 
with  notes  on  other  fossils. 

On  the  geology  of  Arisaig,  Nova 

Scotia,  with  a note  by  Prof.  T.  Rupert 
Jones. 

In  Quart.  Jour.  Geol.  Soc.  London,  vol.  26, 
1870,  P.4‘90. 

The  note  by  Prof.  T.  E.  Jones,  on  p.  492,  on 
some  Entomostraca  from  Arisaig,  mentions  the 
following  genera : 

Beyrichia,  Leperditia,  Primitia. 

Notes  of  examination  by  Prof.  James 

Hall  of  the  Silurian  collection  of  the 
Provincial  Museum,  by  the  Rev.  D. 
Honeyman. 

In  Proc.  and  Trans.  Nova  Scotian  Inst.  Nat. 
Sci.,  vol.  7,  pt.  1,  1886,  p.  14. 

Asaphus  ditmarsice  Honeyman. 

The  Giant  Trilobite  of  Moose  River 

Iron  Mine,  Nova  Scotia. 

In  Proc.  and  Trans.  Nova  Scotian  Inst.  Nat. 
Sci.,  vol.  7,  pt.  1, 1888,  p.  63. 

In  this  article  Dr.  D.  Honeyman  refers  Asa- 
phus ditmarsice  to  Dr.  Jacob  Green’s  Asaphus? 
crypturus,  giving  a copy  of  the  original  descrip- 
tion of  that  species  from  Trans.  Geol.  Soc. 
Pennsylvania,  vol.  1,  pt.  1,  1834,  p.  37. 

How  (Henry).  Notice  of  the  occurrence 
of  a Trilobite  in  the  Lower  Carbonifer- 
ous limestone  of  Hants  County. 

In  Proc.  and  Trans.  Nova  Scotian  Inst.  Nat.  | 
Sci.,  vol.  1, 1867,  pt,  1,  p.  87. 

Hutton  (F.  W.)  On  a Trilobite  from  New  j 
Reefton,  New  Zealand  new  to  Australia,  j 

In  Proc.  Linn.  Soc.  New  South  Wales,  sec- 
tion 2,  vol.  2,  1887-’88,  p.  257. 

.Huxley  (T.  H.)  Observations  ou  the 
structure  and  affinities  of  Himanlopte- 
ru8. 

In  Quart.  Jour.  Geol.  Soc.  London,  vol.  12,  j 
1856,  p.  34. 


Huxley  (T.  H)  and  Salter  (J.  W.)  Mono- 
graph of  the  fossil  Crustacea  forming 
the  genus  Pterygotus,  with  its  anatomy 
and  affinities. 

In  Mem.  Geol.  Survey  United  Kingdom.  De- 
scription of  Brit,  organic  remains.  Monograph 
No.  1.  London,  1859,  atlas  of  16  pis. 

and  Etheridge  (Robert).  A cata- 
logue of  the  collection  of  fossils  in  the 
Museum  of  Practical  Geology,  with  an 
explanatory  introduction.  London, 
1865. 

A catalogue  of  the  Cambrian  and 

Silurian  fossils  in  the  Museum  of  Prac- 
tical Geology.  London,  1878. 

This  catalogue  was  drawn  up  by  Mr.  E.  T. 
Newton,  under  Prof.  T.  H.  Huxley’s  superin- 
tendence. 

The  specimens  were  named  by  Mr.  Kobert 
Etheridge,  palaeontologist  to  the  Geological 
Survey  of  Great  Britain. 

Jackson  (Charles  T.)  Nouveau  gisement 
de  Trilobites  ddcouvert  pres  de  Boston. 

In  Comptes  Eendus  Acad.  Sci.  Paris,  vol.  43, 
1856,  p.  883. 

Paradoxides  tessini,  P.  harlani , P.  spinu- 
losus. 

Sur  un  moule  du  Paradoxides  harlani. 

In  Comptes  Eendus  Acad.  Sci.  Paris,  vol.  46, 
1858,  p.  254. 

James  (J.  F.)”^  Catalogue  of  fossils  of 
Cincinnati  group,  published  by  order 
of  the  Committee  on  Palaeontology. 
Cincinnati,  1871. 

James  (U.  P.)  Paleontology.  Cata- 
logue of  Lower  Silurian  fossils  of  Cin- 
cinnati group,  found  at  Cincinnati  and 
vicinity,  etc.  Cincinuati,  April,  1875. 

Supplement  to  Catalogue  of  Lower 

Silurian  fossils  of  the  Cincinnati  group, 
etc.  Cincinnati,  July  10,  1879. 

Descriptions  of  new  species  of  fossils 

from  the  Cincinnati  group,  Ohio  and 
Kentucky. 

Iu  The  Palaeontologist,  Cincinnati,  No.  7, 
April  16,1883. 

Tracks  of  Crustacean  (?),  pi.  2,  fig.  4. 

Johnstrup  (Fr.)  Oversigtover  de  paleo* 
zoiske  Dannelser  paa  Bornholm  meddelt 
paa  det  llte  Skaudinaviske  Natur- 
forskermede  i Kjobenhavn,  1873,  p.299. 

Jones  (T.  Rupert).  On  Permian  Ento- 
mpstraca. 

In  Monograph  of  Permian  Fossils  of  Eng- 
land (King),  Palaeont.  Soc.  London,  vol.  3, 

• 1849-’54,p.  58. 

Cythere. 


VOGDKS.J 


LIST  OF  AUTHORS. 


39 


Jones  (T.  Rupert)— Continued. 

Notes  on  tbe  Entomostraca. 

In  Quart.  Jour.  Geol.  Soc.  London,  vol.  9, 
1853,  p.  160,  pi.  7,  figs.  5-7. 

Beyrichia. 

This  article  forms  Appendix  D to  a paper  on 
the  Carboniferous  and  Silurian  formations  of 
the  neighborhood  of  Bussaco,  in  Portugal,  by 
Senhor  Carlos  Ribeiro,  with  notes  and  a de- 
scription of  the  animal  remains  by  D.  Sharpe, 
T.  W.  Salter,  and  T.  R.  Jones,  etc.  See  same 
journal,  p.  135,  pis.  7-9. 

Notes  on  tlie  Palaeozoic  bivalved 

Entomostraca.  No.  1.  Some  species 
from  the  Upper  Silurian  limestone  of 
Scandinavia. 

In  Annals  Mag.  Nat.  Hist.,  2d  series,  Lon- 
don, vol.  16, 1855,  p.  81,  pi.  5. 

Beyrichia. 

Notes  on  Palaeozoic  bivalved  Ento- 
mostraca. No.  2.  Some  British  and  for- 
eign species  of  Beyrichia. 

In  Annals  Mag.  Nat.  Hist.,  2d  series,  Lon- 
don, vol.  16, 1855,  p.  163,  pi.  6. 

Beyrichia. 

■ Notes  on  Palaeozoic  bivalved  Euto- 

mostraca.  No.  3.  Some  species  of  Leper- 
ditia. 

In  Annals  Mag.  Nat.  Hist.,  2d  series,  Lon- 
don, vol.  17, 1856,  p.  81,  pis.  6-7. 

Leperditia. 

Notes  on  the  Palaeozoic  bivalved 

Entomostraca.  No.  4.  North  American 
species. 

In  Annals  Mag.  Nat.  Hist.,  3d  series,  London, 
vol.  1,  1858, p.244,  pis.  9, 10.  See,  also,  Rogers’s 
Final  Rept.  Geol.  Survey  Pennsylvania,  1858, 
pt.  2,  p.  834,  figs.  695-699. 

Additional  notes  on  Palaeozoic  Ento- 
mostraca from  Canada. 

In  Annals  Mag.  Nat.  Hist.,  3d  series,  London, 
vol.  1,  1858,  p.  340. 

Leperditia , Isochilina. 

On  the  Palaeozoic  Entomostraca  of 

Canada. 

In  Geol.  Survey  Canada,  figure  and  descrip- 
tion of  Canadian  organic  remains,  decade  3, 
Montreal,  1858,  p.  91,  pi.  2;  also  Annals  Mag. 
Nat.  Hist.,  3d  series,  London,  vol.  1, 1858,  p.  244, 

pi.  9. 

. Beyrichia , Leperditia , Isochilinia  n.  g.,  Cy- 

theropsis. 

Explanation  map  32.  The  geology 

of  the  neighborhood  of  Edinburgh,  by 
H.  II.  Howell  and  A.  Geikie  ; with  ap- 
pendix and  list  of  fossils,  by  J.  W. 
Salter. 

In  Mem.  Geol.  Survey  Gt.  Brit.,  London,  1861, 
p.  137,  pi.  2,  fig.  5. 


Jones  (T.  Rupert)— Continued. 

Prof.  T.  Rupert  Jones  herein  uses  the  name 
of  Entomis  for  certain  fossils.  For  a full  ge- 
neric description,  see  Annals  Mag.  Nat.  Hist., 
4th  series,  London,  vol.  11,  1873,  p.  413. 

A monograph  of  the  fossil  Estherice. 

In  Paljcont.  Soc.  London,  vol.  14, 1862, 134  pp., 

5 pis. 

Estheria,  Leaia  n.  g.,  Beyrichia , Candona, 
Cypridea. 

Note  on  Esiheria  niddendorjii. 

In  Quart.  Jour.  Geol.  Soc.  London,  vol.  19, 
1863,  p.  73. 

On  fossil  Esiheria  and  their  distribu- 
tion. 

In  Quart.  Jour.  Geol.  Soc.  London,  vol.  19, 
1863,  p.  140;  also  Nat.  Hist.  Review,  1863,  p.  262. 

and  Kirkby  (J.  W.)  Notes  on  the 

Palaeozoic  bivalved  Entomostraca.  No. 

5. 

In  Annals  Mag.  Nat.  Hist.,  3d  series,  London, 
vol.  15, 1865,  pi.  20,  p.  404. 

Leperditia,  Gytherella,  Bairdia,  Cythere. 

and  Holl  (H.  B.)  Notes  on  the  Pa- 
laeozoic bivalved  Entomostraca.  No.  6. 

In  Annals  Mag.  Nat.  Hist.,  3d  series,  London, 
vol.  15, 1865,  p.  414,  pi.  13. 

Primitia  n.  g. 

and  Kirkby  (J.  W.)  Notes  on  Pa- 
laeozoic bivalved  Entomostraca.  No.  7. 

In  Annals  Mag.  Nat.  Hist.,  3d  series,  London, 
vol.  18, 1866,  p.  32. 

Entomoconchus,  Daphnia,  Bairdia,  Cythere. 

and  Holl  (W.  B.)  Notes  on  Palaeo- 
zoic bivalved  Entomostraca.  No.  8. 
Some  Lower  Silurian  species  from  Chair 
of  Kildare,  Ireland. 

In  Annals  Mag.  Nat.  Hist.,  4th  series,  Lon- 
don, vol.  2, 1868,  p.  54,  pi.  7. 

Primitia,  Cythere,  Bairdia. 

and  Holl  (H.  B.)  Notes  on  Palaeo- 
zoic bivalved  Entomostraca.  No.  9. 

In  Annals  Mag.  Nat.  Hist.,  4th  series,  Lon- 
don, vol.  3, 1869,  p.  211,  pis.  14, 15. 

Cythere,  Bairdia,  Beyrichia , Primitia,  Thlip- 
sura  n.  g.,  p.  213;  Cytherellina  n.  g.,  p.  215; 
Kirkby  a n.  g , Movea  n.  g.,  JEchmina  n.  g.,  p. 
217. 

On  ancient  Water-fleas  of  the  Ostra- 

codous  and  Phyllopodous  tribes  (bi- 
valved Entomostraca). 

In  Month.  Microsc.  Jour.,  vol.  4,  London, 
1870,  p.  184,  pi.  61. 

Leperditia,  Bairdia,  Thlipsura , Cythere,  Gy - . 
therelta,  Cytherellina,  JEchmina,  Carbonia,  Oy- 
pridina,  Cypridella,  Cyprella , Entomoconchus, 
Entomis,  Primitia,  Kirkbya,  Moorea,  Jsochili- 
nia,  Beyrichia,  Leaia,  Esiheria. 


[BULL.  63. 


40  A BIBLIOGRAPHY  OF  PALEOZOIC  CRUSTACEA. 


Jones  (T.  Rupert) — Continued. 

On  some  bivalved  Entomostraca  j 

from  the  Coal  Measures  of  South  Wales. 
In  Geol.  Mag.,  vol.  7,  1870,  p.  214,  pi.  9. 
Cytheroid  Entomostraca. 

On  the  Palaeozoic  bivalved  Ento- 
mostraca. 

In  Proc.  Geologist  Assoc.,  1870. 

Note  on  the  Entomostraca  from  the 

Cambrian  rocks  of  St.  David’s. 

In  Quart.  Jour.  Geol.  Soc.  London,  vol.  28, 

1872,  p.  183,  pi.  5. 

Leperditia,  Entomis.  Larval  trilobite  ? 

This  paper  forms  a part  of  Henry  Hicks’s  ar- 
ticle on  some  un described  fossils  from  the  Me- 
nevian  Group.  Same  Jour.,  p.  173. 

Notes  on  the  Palaeozoic  bivalved  En- 
tomostraca. No.  10. 

In  Annals  Mag.  Nat.  Hist.,  4th  series,  Lon- 
don, vol.  11,  1873,  p.  413. 

Entomis,  Entomidella  n.  g. 

— On  some  bivalved  Entomostraca, 
chiefly  Cypridenidae  of  the  Carbonifer- 
ous formations. 

In  Quart.  Jour.  Geol.  Soc.  London,  vol.  29, 

1873,  p.  409. 

Sulcuita  n.  g.,  Cyprella. 

Ancient  Water-fleas,  etc.  Pt.  2. 

In  Monthly  Microsc.  Jour.,  vol.  10,  London, 

1873,  p.  71. 

Cythere,  Thlipsura. 

Notes  on  some  forms  of  British  Ento- 
mostraca from  the  Silurian  rocks  of 
Peeblesshire. 

In  Trans.  Edinburgh  Geol.  Soc.,  vol.  2,  pt.  3, 

1874,  p.  321. 

Beyrichia,  Bairdia,  Entomis. 

, Kirkby  (J.  W.)  and  Brady  (M.  P.) 

Monograph  of  British  fossil  bivalve 
Entomostraca  from  the  Carboniferous 
formations. 

In  Palaeont.  Soc.  London,  1874. 

Pt.  1.  The  Cypridinadse  and  their  allies,  5 pis 
Cypridina,  Asterope,  Philomedes , Bradycine- 
tus,  Eurypylus,  Conchcecia,  Halocyris , Hetero- 
desmus , Polycope,  Cytherella,  Cypridinella  n.g., 
Cypridellina  n.  g.,  Gypridella,  Sulcuna,  Cyprella, 
Bhombina  n.  g.,  Entomoconchus,  Off  a n.  g., 
Chadocopa,  Platycopa. 

aud  Kirkby  (J.  W.)  Notes  on  the 

Palaeozoic  bivalved  Entomostraca.  No. 

11. 

In  Annals  Mag.  Nat.  Hist.,  4th  series,  Lon- 
don, vol.  15,  1875,  p.  52,  pi.  6. 

Beyrichia,  Leperditia,  Primitia,  Bairdia,  Cy- 
there. Cytherella. 

Notes  on  some  fossil  bivalved  Ento- 
mostraca. 

In  Geol.  Mag.,  decade 2,  vol.  5, 1878,  p.  100,  pi.  3. 
Esther e,  Cypris,  Candona,  Gypridia. 


Jones  (T.  Rupert)  and  Kirkby  (J.  W.) 
Description  of  the  species  of  the  Ostra- 
codous  genus  Bairdia  McCoy,  from  the 
Carboniferous  strata  of  Great  Britain. 

In  Quart.  Jour.  Geol.  Soc.  London,  vol.  35, 
1879,  p.  565,  5 pis. 

Notes  on  the  Palaeozoic  bivalved 

Entomostraca.  No.  12.  Some  carbonif- 
erous species  belonging  to  the  genus 
Carbonia  Jones. 

In  Annals  Mag.  Nat.  Hist.,  5th  series,  Lon- 
don, vol.  4,  1879,  p.  28,  pis.  2 and  3. 

Carbonia  n.  g. 

Notes  on  the  Palaeozoic  Entomos- 
traca. No.  13.  Entomis  serrato- striata 
and  others  of  the  so-called  Cypridinen 
of  the  Devonian  schist  of  Germany. 

In  Annals  Mag.  Nat.  Hist , 5th  series,  Lon- 
don, 79,  p.  182,  pi.  11. 

Notes  on  some  Palaeozoic  Entomos- 
traca. 

In  Geol.  Mag.,  decade  3,  vol.  8, 1881,  p.  337,  2 
pis. 

Cypridina ?,  Cyprosis,  Leperditia?,  Entomis, 
Primitia,  Beyrichia,  Cyprosina  n.  g.,  Polycope. 

Notes  on  some  Palaeozoic  Entomos- 
traca. No.  14.  Some  Cambrian  and 
Silurian  Leperditia  and  Primitia. 

In  Annals  Mag.  Nat.  Hist , 5th  series,  Lon- 
don, vol.  8,  1881,  p.  332,  pis.  19, 20. 

and  Schmidt  (F.)  On  some  Silu- 
rian Leperditia. 

In  Annals  Mag.  Nat.  Hist.,  5th  series,  Lon- 
don, vol.  9,  1882,  p.  168. 

Notes  on  some  Palaeozoic  bivalved 

Entomostraca.  No.  15. 

In  Annals  Mag.  Nat.  Hist.,  5th  series,  Lon- 
don, vol.  10, 1882,  p.  358,  figs.  1 a,  b. 

Primitia. 

Notes  on  the  Palaeozoic  bivalved 

Entomostraca.  No.  16.  1.  Some  Palaeo- 
zoic and  other  bivalved  Entomostraca 
from  Siberian  Russia,  pi.  6.  2.  Some 

Palaeozoic  bivalved  Entomostraca  from 
Spitzbergen,  pi.  9. 

In  Annals  Mag.  Nat.  Hist.,  5th  series,  Lon- 
don, vol.  12, 1883,  p.  243,  pls.6  and  9. 

Entomis,  Leperditia,  Estheria,  Primitia. 

Notes  on  the  late  Mr.  Tate’s  speci- 
mens of  the  Lower  Carboniferous  Ento- 
mostraca from  Berwickshire,  North- 
umberland. 

In  Proc.  Berw.  Nat.  Club,  vol.  10, 1884, 1 pi. 

Candona ?,  Bemix,  Carbonia,  Macrocypsisf , 
Leperditia,  Beyrichia,  Kirkby  a,  Cythere,  Cythe- 
rella, Estheria,  DarvnneUa  ?. 


VOGDES.] 


LIST  OF 

Jones  (T.  Rupert) — Continued. 

Notes  on  the  Palaeozoic  bivalved 

Entomostraca.  No.  17.  Some  North 
American  Leper ditia  and  allied  forms. 

In  Annals  Mag.  Nat.  Hist.,  5th  series,  Lon- 
don, vol.  14, 1884,  p.  339. 

Leperditia,  Isochilina,  Primilia. 

Report  of  the  committee,  consisting 

of  Mr.  R.  Etheridge,  Dr.  H.  Woodward, 
and  Prof.  T.  Rupert  Jones  (secretary), 
on  the  fossil  Phyllopoda  of  the  Palaeo- 
zoic rocks. 

In  Kept.  53d  Meeting  Brit.  Asso.  Adv.  Sci., 

1883,  p.  215. 

Hymenocari8,  Garyocaris,  Lingulocaris. 

Second  report  of  the  committee  con- 
sisting of  Mr.  R.  Etheridge,  Dr.  H. 
Woodward,  and  Prof.  T.  Rupert  Jones 
(secretary),  on  the  fossil  Phyllopoda  of 
the  Palaeozoic  rocks. 

In  Kept.  54th  Meeting  Brit.  Assoc.  Adv.  Sci., 

1884.  p.  75;  Geol.  Mag.,  n.  s.,  decade  2,  vol.  10, 
1883,  p.  461. 

and  Kirkby  (J.  W.)  On  some  Car- 
boniferous Entomostraca  from  Nova 
Scotia. 

In  Geol.  Mag.,  n.  s.,  decade  3,  vol.  1,  1884,  p. 
356,  pi.  12. 

Leperditia , Beyrichia,  Carbonia,  Candona ?, 
Cythere,  Estheria,  Leaia,  Primitia  or  Beyrichia. 

and  Woodward  (Henry).  On  some 

Palaeozoic  Phyllopoda. 

In  Geol.  Mag.,  n.  s.,  decade  3,  vol.  1,  1884,  p. 
348. 

Discinocaris , Spathiocaris,  Pholadocaris,  Lis- 
gocaris,  Ellipsocaris.  Cardiocaris,  Dipterocaris, 
Pterocari8,  Orescentilla,  Aptychopsis,  Peltocaris, 
Pinnocaris. 

Notes  on  the  Palaeozoic  bivalved  En- 

tomostraca.  No.  18.  Some  species  of 
the  Entomididae. 

In  Annals  Mag.  Nat.  Hist.,  5th  series,  Lon- 
don, vol.  14. 1884,  p.  391,  pi.  15. 

Entomis , Bolbozoe,  Entomidella. 

and  Woodward  (Henry).  Notes 

on  the  British  species  of  Ceratiocaris. 

In  Geol.  Mag.,  n.  s.,  decade  3,  vol.  2,  1885,  p. 
385,  pi.  10.  Continued,  ibid.,  p.  460. 

Kirkby  (J.  W.)  Notes  on  Palaeozoic 

bivalved  Entomostraca.  No.  19.  On 
some  Carboniferous  species  of  the  Os- 
tracodous  genus  Kirkby  a. 

In  Annals  Mag.  Nat.  Hist.,  5tli  series,  Lon- 
don, vol.  15,  1885,  p.  174,  pi.  3. 

and  Holl  (H.  B.)  Notes  on  the 

Palaiozoic  bivalved  Entomostraca.  No. 
20.  On  the  genus  Beyrichia  and  some 

new  Bpecies. 


AUTHORS.  41 

Jones  (T.  Rupert)  and  Holl  (H.  B.)— 
Continued. 

In  Annals  Mag.  Nat.  Hist.,  5th  series,  Lon- 
don, vol.  17, 1886,  p.  337,  pi.  12. 

Beyrichia , Bollia  n.  g.,  Kloedenia  n.  g. 

Notes  on  the  Palaeozoic  bivalved 

Entomostraca.  No.  21.  On  some  Silu- 
rian genera  and  species. 

In  Annals  Mag.  Nat.  Hist.,  5th  series,  Lon- 
don, vol.  17, 1886,  p.  403,  pis.  13, 14. 

Strepula  n.  g.,  Bollia,  Placentula  n.  g.,  Pri- 
mitia. 

and  Kirkby  (J.  W.)  Notes  on  the 

distribution  of  the  Ostracoda  of  the 
Carboniferous  formation  of  the  British 
Isles. 

In  Abstracts  Proc.  Geol.  Soc.  London,  ses- 
sion 1885-86,  No.  489,  p.  86. 

On  Carboniferous  Ostracoda 

from  the  Gayton  borings,  Northamp- 
tonshire. 

In  Geol.  Mag.,  n.  s.,  decade  3,  vol.  3,  London, 
1886,  p.  248,  pi.  7. 

Kirkbya,  Bythocypris , Macrocypris,  Cythe- 
rella. 

Notes  on  the  Palaeozoic  bivalved 

Entomostraca.  No.  22.  On  some  unde- 
scribed species  of  British  Carbonilerous 
Ostracoda. 

In  Annals  Mag.  Nat.  Hist.,  5th  series,  Lon- 
don, vol.  18,  1886,  p.  249,  pis.  6-9. 

Bythocypris,  Cythere  ?,  Leperditia,  Beyrichia, 
Primitia?,  Beyrichiella?,  Kirkbya,  Moorea,  Cy- 
therella,  Bathocythere,  Argillcecia,  Aglaia?, 
Xestoleberis  ?,  Macrocypris,  Carbonia,  Bairdia. 

On  some  fringed  and  other  Os- 
tracoda from  the  Carboniferous  series. 

In  Geol.  Mag.,  n.  s.,  decade  3,  vol.  3,  London, 
1886,  p.  434,  pis.  11, 12. 

Beyrichiopsis  n.  g.,  Beyrichiella  n.  g.,  Bey- 
richia. 

On  Palaeozoic  Phyllopoda. 

In  Geol.  Mag.,  n.  s.,  decade  3,  vol.  3,  London, 
1886,  p.  456. 

Ceratiocaris. 

Notes  on  the  distribution  of  the 

Ostracoda  of  the  Carboniferous  forma- 
tions of  the  British  Isles. 

In  Quart.  Jour.  Geol.  Soc.  London,  vol.  42, 
1886,  p.  496. 

Beyrichiopsis , Phreatura  n.  g.,  Youngia  n.  g. 

This  generic  name  was  used  tor  a new  genus 
of  Tlilobites  by  Lindstrbm  in  1885. 

Note. — Since  this  paper  was  read  many  of  the 
species  have  been  described  and  figured  in  the 
Annals  Mag.  Nat.  Hist,  for  October,  1886,  and 
in  the  Geol.  Mag.  of  the  same  date.  Others  in 
tbe  Proc.  Geologist  Assoc.,  vol.  9,  1886. 

Fourth  report  of  the  committee,  con- 
sisting of  Mr.  Ii.  Etheridge,  Dr.  H. 


42 


A BIBLIOGRAPHY  OF  PALEOZOIC  CRUSTACEA. 


[bull.  63. 


Jones  (T.  Rupert) — Continued. 
Woodward,  and  Prof.  T.  Rupert  Jones 
(secretary),  on  the  fossil  Phyllopoda  of 
the  Palaeozoic  rocks,  1886. 

In  Kept.  56th  Meeting  Brit.  Assoc.  Adv.  Sci., 

1886,  p.  229. 

Ceratiocaris , Emmelezoe , Xiphocaris,  Physo- 
car  is,  Cryptozoe. 

and  Kirkby  (James  W.)  A list  of 

the  genera  and  species  of  bivalved  En- 
tomostraca  found  in  the  Carboniferous 
formations  of  Great  Britain  and  Ireland. 
With  notes  on  the  genera  and  their 
distribution. 

In  Proc.  Geologist  Assoc.,  vol.  9, 1886,  p.  495. 

I.  Cypridinidse : 1.  Cypridina,  2.  Cypridi- 
nella,  3.  Cypridellina,  4.  Cypridella,  5.  Sulcuna, 
6.  Cyprella,  7.  JBradycinetus,  8.  Philomedes,  9. 
Rhombina.  II.  Entomoconchidse : 1.  Entomo- 
conchus,  2.  Offa.  III.  Polycopidae : 1.  Polycope. 
IY.  Entomididae:  1.  Entomis.  V.  Cytherel- 
lidas : 1.  Cytherella.  YI.  Leperditiidae : 1.  Le- 
perditia,  2.  Bernix,  3.  Beyrichia , 4.  Beyrichiella, 
5.  Beyrichiopsis,  6.  Eirkbya,  7.  Moorea,  8. 
Phreatura.  VII.  Cyprididae:  1.  Aglaia , 2. 
Candona,  3.  Argillcecia,  4.  Macrocypris,  5.  By- 
thocy prise  .6.  Bairdia.  VIII.  Dawmulidse:  1. 
Daivinula.  IX.  Cytheridas:  1.  Cythere , 2. 
Xestoleberis , 3.  Bythocythere,  4.  Carbonia,  5. 
Youngia. 

, Etheridge  ( R.  ) and  Woodward 

(H.)  Fifth  report  of  the  committee, 
consisting  of  Mr.  R.  Etheridge,  Dr.  H. 
Woodward,  and  Prof.  T.  Rupert  Jones 
(secretary),  on  the  fossil  Phyllopoda  of 
the  Palaeozoic  rocks,  1887. 

In  Kept.  57th  Meeting  Brit.  Assoc.  Adv.  Sci., 

1887,  p.  60. 

Ceratiocaris,  Dithyrocaris,  Leaia,  Estheria. 

Notes  on  the  Palaeozoic  bivalved 

Entomostraca.  No.  23.  On  some  Silu- 
rian genera  and  species  (continued). 

In  Annals  Mag.  Nat.  Hist.,  5th  series,  Lon- 
don, vol.  19,  1887,  p.  117,  pis.  4-7. 

Macrocypris,  Pontocypris,  Bythocypris,  Cy- 
there, CytliereUa , Primitia. 

Prof.  T.  Kupert  Jones  remarks  in  this  paper : 
“Now  that  not  only  Cythere  hut  its  allied 
genera  have  been  fully  elucidated  in  the  living 
state,  it  is  found  that  the  genus  does  not  com- 
prehend many  of  the  fossil  forms  once  referred 
to  it.  Whether  these  really  belong  to  the 
Cytheridce  or  to  the  Cyprididae  it  is  often  diffi- 
cult to  say ; hut  the  genus  Cythere  comprises 
very  few  of  the  smooth  suhovate  forms,  and 
none  that  have  toothless  hinges.  Hence  we 
find  that  a real  Cythere  is  scarcely  known  in 
Paheozoic  strata.” 

Notes  on  the  Palaeozoic  bivalved  En- 
tomostraca. No.  24.  On  some  Silurian 
genera  and  species  (continued). 


Jones  (T.  Rupert) — Continued. 

In  Annals  Mag.  Nat.  Hist.,  5th  series,  Lon- 
don, vol.  19, 1887,  p.  400,  pis.  12, 13. 

Thlipsura,  Octonaria  n.  g.,  Bollia,  Primitia, 
Moorea,  Xestoleberis,  Achmina. 

Notes  on  some  Silurian  Ostracoda 

from  Gothland.  Stockholm,  1887, 8 pp. 

Beyrichia,  Leperditia,  Primitia,  Primitiopsis 
n.  g.,  Macrocypris,  Bythocypris . Thlipsura,  Ach- 
mina, Bursulella  n.  g. 

Notes  on  the  Palaeozoic  bivalved  En- 
tomostraca. No.  25.  On  some  Silurian 
Ostracoda  from  Gothland. 

In  Annals  Mag.  Nat.  Hist.,  6th  series,  Lon- 
don, vol.  1, 1888,  p.  395. 

Beyrichia,  Leperditia,  Entomis,  Primitia, 
Primitiopsis  n.  g.,  Macrocypris,  Bythocypris, 
Thlipsura,  Achmina,  Bursulella  n.  g. 

Notes  on  the  Palaeozoic  bivalved  En- 
tomostraca. No.  26.  On  some  new  De- 
vonian Ostracoda,  with  a note  on  their 
geological  position,  by  the  Rev.  G.  F. 
Whidborue. 

In  Annals  Mag.  Nat.  Hist.,  6th  series,  Lon- 
don, vol.  2, 1888,  p.  295, 1 pi. 

Kyamodes  n.  g. 

and  Woodward  (Henry).  A mono- 
graph of  the  British  Palaeozoic  Phyllo- 
poda (Phyllocarida,  Packard). 

In  Palaeont.  Soc.  London,  vol.  41, 1887,  pt.  1. 

Ceratiocaridce. 

On  some  Scandinavian  Phyllo- 

caridaB. 

In  Geol.  Mag.,  n.  s.,  decade  3,  vol.  5,  London, 
1888,  p.  97,  pi.  5. 

Ceratiocaris. 

and  others.  Sixth  report  of  the  com- 
mittee, consisting  of  Mr.  E.  Etheridge, 
Dr.  H.  Woodward,  and  Prof.  T.  Rupert 
Jones  (secretary),  on  the  fossil  Phyllo- 
poda of  the  Palaeozoic  rocks,  1888. 

In  Kept.  58th  Meeting  Brit.  Assoc.  Adv.  Sci., 

1888. 

Ceratiocaris,  Echinocaris,  Equisitides,  Ely- 
mocaris,  Tropidocaris,  Mesothyra,  Dithyrocaris, 
Rhinocaris,  Spathiocaris,  Dipterocaris,  Esthe- 
ria, Hymenocaris,  Saccocaris,  Lingidocaris, 
Bactropus,  Schizodiscus. 

Author’s  edition,  9 pp.  and  9 wood-cuts. 

and  Woodward  ( Henry ).  See 

Woodward  (Henry)  and  Jones  (T. 
Rupert). 

See  Schmidt  (Fr.)  and  Jones  (T. 

Rupert). 

Jordan  (H.)  Ueberreste  eines  kleinen 
iiberaus  merkwiirdigen  Crustacees. 


VOGDES.] 


LIST  OF  AUTHORS. 


43 


Jordan  (H.) — Continued. 

In  Yerhandl.  natur.  Vereins  preussischen 
Rheinlande,  Jahrg.,  vol.  4,  1847,  p.  89,  pi.  2, 
figs.  1,  2. 

Gampsonyx  (von  Meyer)  n.  g. 

and  Meyer  (H.  yon).  Ueber  die 

Crustaceen  der  Steinkoblenformation 
von  Saarbriicken.  Cassel,  1854,  2 pis. 

Gampsonyx,  Adelophthalmus  (Eurypterus), 
Chonionotus,  Arthropleura. 

Jukes  (F.)  and  Sowerby  (J.  D.  C.)  An 
account  of  a new  species  of  Trilobite 
found  in  the  Barr  limestone  in  the 
neighborhood  of  Birmingham,  by  Fred- 
erick Jukes,  with  a note  by  J.  D.  C. 
Sowerby. 

In  Mag.  Nat.  Hist.  (London),  vol.  2,  London, 
1829,  p.  41,  5 figs. ; Am.  Jour.  Sci.,  1st  series, 
vol.  23,  1833,  p.  203;  Nenes  Jahrbuch  fur  Mi- 
neral., 1833,  p.  624. 

( Bumastes  barriensis),  Asaphus , Calymene. 

Karsten  (Gustav).  Die  Versteiuerungen 
des  Uebergangs-Gebirges  in  den  Ge- 
rollen  der  Herzogthumer  Schleswig  und 
Holstein.  Kiel,  1869,  25  pis. 

Olenu8.  Proetu8,  Cyphaspis , Phacops,  Caly- 
rnene,  Lichas,  Trimicleus,  Ampyx,  Asaphus, 
Isotelus,  Cerauru8,  Sphcerexochus,  Encrinurus, 
Nileus,  Agnostus,  Beyrichia,  Cy there. 

Kayser  (Emanuel).  Beitrage  zur  Geolo- 
gie  und  Paheontologie  der  Argentini- 
schen  Republik.  Cassel,  1876,  2 pis. 

Olenus.  Arionellus,  Bathyurus?,  Arethusina, 
Ampyx , Asaphus,  Ogygia,  Agnostus , Leperditia. 

Die  Fauna  der  altesten  Devonbildun- 

gen  des  Harzes. 

In  Abhandlungen  zur  geologisctafcn  Special- 
karte  von  Preussen  und  den  thuringischen 
Staaten.  Vol.  2,  pt  4.  Berlin,  1878.  Atlas,  36 
pis. 

Harpe8,  Proelus,  Cryphceus,  Cyphaspis , Pha- 
cops, Dalmanites , Lichas,  Acidaspis , Bronteus, 
Primitia,  Dithyrocaris. 

Ueber  Dalmanites  rhenanus , eine  Art 

der  HaMsmanni-Gruppe,  und  einige  au- 
dere  Trilobiten  aus  den  alteren  rhei- 
nischen  Dachschiefern. 

In  Zeitscbr.  Deutscb.  geol.  Gesell.,  vol.  32, 
1880,  p.  19,  pi.  3. 

Phacops,  Cryphceus , Dalmanites. 

Dechenella,  eine  devonische  Gruppe 

der  Gattung  Phillipsia. 

In  Zeitschr.  Deutsch.  geol.  Gesell.,  vol.  32, 
1880,  p.  703,  pi.  27. 

Dechenella  n.  g. 

Beitrage  zur  Kenntniss  von  Oberde- 

von  und  Culm  am  Nordrande  des  rhei- 
nischen  Schiefergebirges;  Arten  aus 
dem  Culm  von  Aprath. 


Kayser  (Emanuel) — Continued. 

In  Jahrbuch  Preuss.  geol.  Landesanst.  und 
Bergakad.,  Berlin,  1881,  p.  67. 

Phillipsia  cequalis,  P.  longicornis,  P.  eich- 
waldi,  P.  emarginata. 

Die  Orthocerasschiefer  zwischen 

Balduinstein  und  Laurenberg  an  der 
Lahn.  Palaeontologischer  Anhang. 

In  Jahrbnch  Preuss.  geol.  Landesanst.  und 
Bergakad.,  Berlin,  1883,  p.  34,  pi.  3,  fig.  6. 

Phacops  fecundus,  Cryphceus  rotundi/rons , , 
C.  kochi. 

Mittel-  und  obersilurische  Verstei- 
uerungen aus  dem  Gebirgsland  von 
Tshau  Tiens. 

In  Chipa  (Richthofen),  vol.  4,  Berlin,  1883, 
p.  37. 

Asaphxis,  Calymene,  Trinucleus  richthofeni, 
Encrinurus. 

Obercarbonische  Fauna  von  Loping. 

In  China  (Richthofen),  vol.  4,  Berlin,  1883,  p. 
161. 

Phillipsia  obtusicauda , pi.  19,  fig.  3. 

Keyes  (Chas.  R.)  On  the  fauna  of  the 
Lower  Coal  Measures  of  central  Iowa. 

In  Proc.  Acad.  Nat.  Sci.  Phila.,  1888,  p.  222. 

Cythere  nebracensis. 

Kiesow  (J.  von).  Ueber  silurische  und 
devonische  Geschiebe  West-Preussens. 

In  Schrift.  nat.  Gesell.  Danzig,  new  series, 
vol.  6, 1884,  p.  205,  3 pis. 

Proetus,  Phacops,  Calymene,  Lichas, Ampyx, 
Asaphus,  Ptychopyge,  Illoenus.  Acidaspis, 
Cheirurus,  Encrinurus,  Beyrichia,  Leperditia, 
Primitia,  Cytherellina. 

Ueber  gotlandische  Beyrichien. 

In  Zeitschr.  Deutsch.  geol.  Gesell.,  vol.  40, 
1888,  p.  1,  2 pis. 

Kinnear  ( W.  T. ) Note  on  the  occurrence 
of  a new  Carboniferous  Crustacean  at 
Ardrois  Castle,  Fife. 

In  Trans.  Edinburgh  Geol.  Soc.,  vol.  5,  pt.  3, 
1887,  p.  417. 

Dithyrocaris,  Palceocrangon,  Ceratiocaris, 
Rostrocaris  n.  g. 

Kinsky  (Gra/ von).  Schreiben  des  H. 
Grafen  von  Kinsky  an  von  Born  iiber 
einige  mineralogische  und  lithologische 
Merk  wiirdigkeiten . 

In  Abhandlungen  einer  Privat-Gesell.  in  Boh- 
men,  vol.  1,  Prag,  1775,  p.  243. 

Kirkby  ( J.  W. ) On  some  Permian  fos- 
sils from  Durham. 

In  Trans.  Tyneside  Nat.  Field  Club,  vol.  3, 
1858,  p.  286. 

On  Permian  Entomostraca  from  the 

shell  limestone  of  Durham.  With  notes 
on  the  species  by  T.  Rupert  Jones. 


44  A BIBLIOGRAPHY  OF  PALEOZOIC  CRUSTACEA.  [bull.  63. 


Kirkby  (J.  W.)— Continued. 

In  Annals  Mag.  Nat.  Hist.,  3d  series,  Lon- 
don, vol.  2, 1858,  p.  317,  4 pis. 

Kirkbya,  Gytheridce,  Cythere,  Bairdia. 

— - and  Jones  (T.  Rupert).  On  Per- 
mian Entomostraca. 

In  Trans.  Tyneside  Nat.  Field  Club,  vol.  4, 
1859,  p.  122,  4 pis. 

See,  also,  Jones  (T.  Rupert)  and  Kirkby  (J. 
W.),  and  Jones  (T.  Rupert),  Kirkby  (J.  W.), 
and  Brady  (M.  P.). 

On  the  Permian  rocks  of  Sou  tli  York- 
shire and  their  Palaeontological  rela- 
tions. 

In  Quart.  Jour.  Geol.  Soc.  London,  vol.  17, 
1861,  p.  287. 

Cythere  (Bairdia),  Kirkbya. 

On  some  additional  species  that  are 

common  to  the  Carboniferous  and  Per- 
mian strata. 

In  Annals  Mag.  Nat.  Hist.,  3d  series,  Lon- 
don, vol.  10, 1862,  p.  202. 

Kjerulf  (Theo. ) Yeiviser  ved  geologiske 
Exkursioner  i Christiania  og  Omegn. 
Christiania,  1865. 

The  author  herein  gives  a list  of  Norwegian 
Silurian  fossils,  with  some  notes  and  figures  on 
the  genera  Ceratopyge,  Cyrtometopus,  Illcenus, 
Phacops. 

Klein  (J.  T.)  Specimen  descriptionis 
petrefactorum  Gedanensium  order  Ory  c- 
tographia  Gedannensis,  etc.  (*) 

In  Nuremberg,  1770,  folio,  pi.  15,  figs.  5-7. 

Calymene  blumenbachii. 

Kloden  (K.  F.)  Die  Yersteinerungen  des 
Mark  Brandenburg,  etc.  Berlin,  1834, 
10  pis. 

Cytherina  phaseolus  Calymene  blumen- 
bachii, C.  var . tuber culata,  C.  var .pulchella,  C. 
sclerops,  C. punctata,  C.  concinna,  C.polytoma?, 
Asaphus  extenuatus? , A.  angustifrons,  A.  ex - 
pansus,  A.  auriculatus,  A.  dilatatus,  A.  (I  lice- 
nus)  crassicauda,  A.  ( Ampyx ) nasutus?,  A.cau- 
datus,  Battus  pisiformis,  B.  tuberculatus,  pi.  1, 
figs.  16-23.  F.  McCoy,  “Brit.  Pal.  Rocks,” p. 
135,  remarks  on  this  species  that  the  name  Bey- 
richia  tuberculatus  is  generally  applied  to  fig. 
22  of  Kloden’s  plate,  which  is  a common  form 
in  the  Gothland  beds) ; Battus  gigas,  pi.  2,  fig.  1. 

Koch  (C.)  Monographie  der  Homalo- 
notus-Arten  des  rheinischen  Unterde- 
von. 

In  Preuss.  geol.  Landesanstalt,  Abhandl., 
Berlin,  1883,  vol.  4,  pt.  2. 

Koenen  (A.  von).  Die  Kulm-Fauna  von 
Herborn. 

In  Neues  Jahrbuch  fur  Mineral.,  1879,  p.  309, 
pis.  6,  7. 

Phillipsia,  Proetus. 


Koenen  (A.  von) — Continued. 

Ueber  die  Unterseite  der  Trilobiten. 

In  Neues  Jahrbuch  fiir  Mineral.,  1880,  vol.  1, 
p.  429,  pi.  8,  figs.  9,  10. 

Phacops,  Asaphus,  Calymene. 

Ueber  Clymenienkalk  und  Mittel- 

Devonien  bei  Montpellier. 

In  Neues  Jahrbuch  fiir  Mineral.,  1886,  p.  163. 

Deckenella  escoli. 

Kolmodin  (Lars).  Bidrag  till  kaune- 
domen  om  Sveriges  Siluriska  Ostra- 
coder. 

In  Akad.  Afhandling  som  med  tillstand  af 
Tidtberomda  Filosofiska  Fakultetens  i Upsala, 
etc.,  1869,  1 pi. 

Leperditia,  Beyrichia,  Gytheropsis,  Pipe. 

Ostracoda  Silurica  Gotlandise  enu- 

merat. 

In  Ofversigt  kongl.  Vet.  Akad.  Forhandlin- 
gar,  1879,  No.  9,  p.  133,  pi  19. 

Leperditia,  Beyrichia,  Elpe. 

Konig  (C.  E.)  leones  fossilium  sectiles. 

Centuria  prima,  text,  4 pp.,  pis  1-8;  Cen- 
turia  seconda,  pis.  9-19. ; n.  d. 

The  common  edition  of  this  work  has  only 
four  pages  of  text  and  eight  plates  (London, 
1820,  4to). 

Calymene  decipiens,  p.  2,  pi.  3,  fig.  32  (Ellipso- 
cephalushoffi) ; Asaphus  my  ops,  p.  3,  pi.  4,  fig.  53; 
Homalonotus  n.  g.,  E.  knighti,  p.4,  pi.  7,  fig.  85; 
Agnostics,  pi.  10,  figs.  119,120;  Isotelus  gigas,  pi. 
10,  fig.  121;  Asaphus  extenuatus,  pi.  10,  fig.  122; 

A.  crassicauda,  pi.  13,  fig.  150;  Belinurus  n.  g., 

B.  bellulus]  pi.  18,  fig.  230. 

For  a description  of  the  genus  Belinurus,  see 
W.  H.  Baily’s  article,  Annals  Mag.  Nat.  Hist., 
3d  series^London,  vol.  11, 1863. 

Koninck  (L.-G.  de).  M6moire  sur  les 
Crustac&s  fossiles  de  Belgique. 

In  Mem.  Acad.  Sci.  Bruxelles,  vol.  14,  1841, 

lpl. 

Goldius  n.  g.,  Asaphus,  Cyclus  n.  g.,  Cythe- 
rina, Cypridina,  Cyprella  n.  g.  (Phillipsia  and 
Bronteus). 

Description  des  animaux  fossiles  qui 

se  trouvent  dans  le  terrain  carboui- 
fere  de  Belgique.  Li&ge,  lH42-’44. 

Cythere,  Cypridina,  Cyprella.  Cypridellan.  g., 
Cyclus,  Phillipsia  brongniarti,  P.  globiceps,  P. 
derbyensis,  P.  gemmulifera,  P.  pustulata,  P. 
jonesii. 

Recherches  sur  les  fossiles  palaeo- 

zoiques  de  la  Nouvelle-Galles  du  Sud 
Australia. 

In  M6m.  Soc.  Sci.  Li6ge,  2d  series,  voL  6, 1877. 

Jllamus,  Staurocephalus,  Cheirurus  Encri- 
nurus,  Gromus,  Calymene,  Proetus,  Lichas, 
Bronteus,  Harpes. 


VOGDE6.]  LIST  OF 

Koninck  (L.-G.  de)— Continued. 

Rechcrckes  sur  les  fossiles  palseo- 

zo'iques  de  la  Nouvelle-Galles  du  Sud 
Australie. 

In  M6m.  Soc.  Sci.  Li&ge,  2d  series,  vol.  7, 1878. 

Phillipsia,  Griffithides,  Brachymetopus. 

Sur  une  nouvelle  espkce  de  crustacd 

du  terrain  houiller  de  la  Belgique. 

In  Bull.  Acad.  Sc.  Bruxelles,  2d  series,  vol. 
45,  1878,  p.  409, 1 pi. 

Brachypyge  carbonis. 

The  principal  part  of  this  article  is  a letter 
from  Dr.  Henry  Woodward  to  L.  G.  de  Koninck. 

Notice  sur  le  Prestwichia  rotundata 

J.  Prestwick,  decouvert  daus  le  sckiste 
kouiller  de  Horrae,  prks  Mona. 

In  Bull.  Acad.  Sci.  Bruxelles,  3d  series,  vol.  1, 
1881,  p.  91, 1 pi. 

Krause  (A.)  Die  Fauna  der  sogen. 
Beyrichien  oder  Ckoneten-Kalke  des 
norddeutscken  Diluviums. 

In  Zeitschr.  Deutsch.  geol.  Gesell.,  vol.  29, 
Berlin,  1877,  p.  1, 1 pi. 

Oalymene  blumenbachii , Phacops  downingce , 
Proetus  concinus,  Leperditia , Beyrichia,  Cythe- 
rellina,  Primitia. 

Kuntgen  (K.)  Die  Trilokiten.  (*) 

In  Mus.  Luxemburg,  1877. 

Kutorga  (S.)  Beitrage  zur  Kenntn.  der 
organiscken  Uekerreste  des  Kupfer- 
aandst.  am  westl.  Abkange  des  Urals. 
St.  Petersburg,  1838,  p.  22,  pi.  4,  figs. 
1-3. 

Limulue  oculatus  Kutorga. 

Edouard  d’Eichwald  (‘  Lethma  Rossica,”  vol. 
1,  p.  1360)  uses  this  species  for  a type  of  his  new 
genus,  Oompylocephalu8. 

Ueber  einige  kaltische  silurische 

Trilokiten. 

In  Verhandl.  russ.  k.  mineral.  Gesell.  zu  St. 
Petersburg,  1847,  p.  287,  plate. 

A8aphu8,  Ill(enu8y  Bncrinurus. 

Einige  Sphcerexochus  und  Cheirurus 

ana  den  ailuriscken  Kalksteiuschickten 
dea  Gov.  St.  Petersburg. 

In  Verhandl.  russ.  k.  mineral.  Gesell.  zu  St. 
Petersburg,  1854,  p.  105, 3 pis. 

Oheirurus  gembnitzkii,  O.  macrophthahnus, 
Sphcerexochus  cranium, , S.  hemicranium,  S. 
platy cranium,  S.  enurus. 

Lang  (C.  N.)  Hiatoria  lapidum  figura- 
torurn  Helvetia  ej  usque  viciute  in  qua 
enarranturomnia  eorurn  genera,  species 
et  vires.  Venetiia,  1708.  (#) 

Tractatus  de  origine  lapidum  figura- 

torum  Helvetia.  Lucernaj,  1700.  (*) 


AUTHORS.  45 

Laspeyres  (H.)  Das  fossile  Pkyllopo- 
den-Genus  Leaia. 

In  Zeitschr.  Deutsch.  geol.  Gesell.,  Berlin, 
1870,  p.  733,  1 pi. 

Latreille  (P.-A.)  Affinit6s  desTrilobites. 

In  Mem.  Mus.  Hist.  Hat.,  Bruxelles,  vol.  7, 
1821,  p.  22 ; Annals  Sci.  Phys.,  Bruxelles,  vol.  6. 

Lawrow  (N.)  Zwei  neue  Asapkus-Arten 
aus  dem  siiuriscken  Kalksteine. 

In  Verhandl.  russ.  k.  mineral.  Gesell.  zu  St. 
Petersburg,  1855-56,  p.  237,  pis.  4,  5. 

Ptycliopyge  und  Megalaspis,  Trilobi- 

ten  der  unter-siluriscken  Kalksteine. 

In  Verhandl.  russ.  k.  mineral.  Gesell.  zu  St. 
Petersburg,  1857-’58,  p.  146,  plate. 

Lebesconte  (M.-P.)  Constitution  g6u.6- 
rale  du  massif  breton  compares  a celle 
du  Finist&re. 

In  Bull.  Soc.  Geol.  France,  3d  series,  vol.  14, 
1886,  p.  776,  pis.  34-36. 

Homalonotus  barroisi , II.  heberti,  Ogygites. 

Lehmann  ( J.  G.  ) Versuck  einer  Ge- 
schickte  von  Flotzgebirgen  betreffeud 
deren  Entstekung,  Lage,  darin  befind- 
licken  Metalle,  Mineralien  und  Fossi- 
lien.  Berlin,  1756.  (*) 

De  Entrockis  et  Asteriis.  (*) 

In  Hovi  Comm.  Sci.  Petropol.,  vol.  10,  1764, 
p.  429,  par.  12,  par.  12,  figs.  8-10. 

Leuchtenberg  (M.  H.  von).  Beschrei- 
bung  einiger  neuer  Tkierreste  der  Ur- 
welt  von  Zarskoje-Selo.  St.  Peters- 
burg, .1843,  2 pis. 

Asaphus,  Nileus , Metopias. 

Lhwyd  (Edward).  Part  of  a letter  from 
Mr.  Edward  Lkwyd  to  Doctor  Martin 
Lister. 

In  Philos.  Trans.  Royal  Soc.  London,  vol.  20, 
No.  243,  1698,  p.  299,  plate,  figs.  8, 9,  and  10. 

This  paper  contains  the  earliest  account  of 
Trilobites.  The  author  discovered  two  frag- 
ments and  one  entire  specimen  of  Ogygia  buchii 
near  Llandeilo,  in  Carmarthenshire.  Lhwyd 
says  in  his  letter  that  he  did  not  know  what  to 
make  of  these  fossils.  The  Ogygia  (fig.  10)  he 
refers  to  the  skeleton  of  an  unknown  fish.  Fig. 
8 represents  the  head  of  a species  of  the  genus 
Trinucleus. 

Litkophylacii  Britannici  Ichnogra- 

phia.  Londiui,  1699,  23  pis.;  2d  ed., 
1760. 

This  work  gives  a catalogue  of  English  fos- 
sils contained  in  the  Ashmolean  Museum,  and 
also  several  essays  on  fossils.  In  the  author’s 
article  “ Epistolal.  delapidibus  quibusdam  Ger- 
mania acceptis,”  pp.  95-100,  he  alludes  to  an 
Ogygia,  and  remarks  : “ This  ichthyomorphous 
stone  swims  spread  out  on  its  side,  although  it 


46 


A BIBLIOGRAPHY  OF  PALEOZOIC  CRUSTACEA. 


[BULL.  63. 


Lhwyd  (Edward) — Continued. 

does  not  correspond  to  any  specimen  heretofore 
discovered;  it  does  not  agree  in  its  external  out- 
line to  your  fossil,  but  represents  the  skeleton 
of  the  same  or  of  a sole,  only  the  specimen  is 
striated  on  the  circumference.  The  figure  be- 
longs to  Buglossium,  or  the  sole  fish,  except  it 
is  somewhat  larger  and  less  compressed  at  its 
extremities,  hut  it  wants  the  tail  of  a fish.  We 
call  it  Buglossam  curtam  strigosam."  He  also 
gives  a description  and  figure  of  Trinucleus  Jim- 
briatum  vulgare , pi.  22,  23,  on  which  It.  I.  Mur- 
chison afterwards  founded  the  genus  Trinucleus. 

Lindaker  ( T.  J.  ) Beschreibung  einer 
noch  nicht  bekannteu  Kafermuschel.  (*) 

In  Mayer’s  Sammlung  phys.  Aufsatze,  Dres- 
den, vol.  1,  1791,  p.  37,  pi.  1. 

The  author  describes  under  the  name  of 
“gegitterte  Kafermuschel”  a Trinucleus  from 
Prague. 

Lindstrom  (G.)  Norminafossilium  Silu- 
riensium  Gotlandiae  Laroverks  program. 
Yisby,  1867. 

Proetus,  Phacops,  Calymene,  Homalonotus, 
Lichas,  Acidaspis,  Trapelocera,  Cheirurus,  Dei- 
phon,  Sphcerexochus,  Oryptonymus , Bronteus, 
BumastMS , Eurypterus,  Pterygotus,  Ceralioca- 
ri8,  Beyrichia , Leperditia,  Gytheropsis. 

List  of  tbe  fossils  of  tbe  Upper  Silu- 
rian formation  of  Gothland.  Stock- 
holm, 1885. 

Forteckning  pa  Gotland  Siluriska 

Crustac^er. 

In  Ofversigt.  Kongl.  Vet.  Akad.  Forhand- 
lingar,  1885,  No.  6,  p.  37,  pis*  12-16. 

Harpes,  Proetus , Cypkaspis,  Phcetonides,  Pha 
cops , Calymene,  Homalonotus,  Lichas,  Trochu- 
rus,  Acidaspis,  Cheirurus , Sphcerexochus,  Youn- 
gia  n.  g , Deiphon,  Encrinurus,  Illcenus , Bron- 
teus, Eurypterus. 

Linnarsson  (J.  G.  O.)  Om  de  Siluriska 
bildningarne  i Mellersta  Westergot- 
land.  1. 

In  Akad.  Afhandling  som  med  tillstand  af 
Vidtberomda  Filosofiska  Fakulten  i Upsala, 
etc.,  1866,  2 pis. 

The  Trilobites  are  .grouped  as  follows : 
Phacopidae:  Phacops.  Cheiruridae:  Pliomera, 
Cyrtometopus,  Sphcerexochus.  Encrinuridae : 
Cybele.  Acidaspidae:  Acidaspis.  Lichidae : ££- 
chas.  Harpedidae : Arraphus.  Calymenidae : 
Calymene,  Homalonotus.  Aulacopleuridae: 
Aulacopleura.  Liostracidae : Liostracus.  Ole- 
nidae : Paradoxides,  Olenus,  Peltura,  Parabo- 
lina,  Eurycare,  Sphcerophthalmus.  Pemo- 
pleurideae:  Remopleurides.  Proetidao:  Forbe- 
sia.  Asapliidae:  Asaphus,  Megalaspis,  Pty- 
chopyge,  Ogygiaf,  Niobe.  Hlaeuidae:  Illcenus , 
Rhodope,  Nilcus,  Symphysurus,  JEglina.  Tri- 
nucleidae:  Trinucleus,  Ampyx , Lonchodomas, 
Raphiophorus,  Dionide.  Aguostidae : Agnos- 
tus.  Incertae  sedis:  Holometopus. 


Linnarsson  (J.  G.  O.) — Continued. 

The  author  also  gives  descriptions  and  fig- 
ures of  the  following  species : Phacops  pulchel- 
lus,  Cyrtometopus  latilobus,  Sphcerexochus  lati- 
ceps,  Lichas  segmentatus,  Ogygia?  apiculata, 
Illcenus  limbatus,  Agnostus  ajfinis. 

Om  Vestergotlands  Cambriska  ocb 

Siluriska  Aflagringar. 

In  Kongl.  Svenska  Vet.-Akad.  Handl.,  vol. 

8,  No.  2,  1869,  2 pis. 

Harpes,  Remopleurides,  Paradoxides,  Dikelo- 
cephalus,  Olenus,  Trigrthrus,  Ceratopyge,  Cono- 
coryphe,  Anomocare,  Arionellus,  Liostracus, 
Euloma,  Holometopus,  Proetus,  Harpides,  Phil- 
lipsia,  Phacops,  Calymene,  Homalonotus,  Lichas, 
Trinucleus,  Ampyx,  Dionide,  Asaphus,  Mega- 
laspis, Symphysurus,  Stygina,  Ogygia,  Niobe,  ~ 
AUglina,  Acidaspis,  Cheirurus,  Sphcerexochus, 
Staurocephalus,  Pliomera,  Cybele,  Encrinurus, 
Dindymene,  Nileus,  Panderia,  Agnostus,  Leper- 
ditia, Beyrichia,  Primitia. 

Diagnoses  specierum  novarum  e 

class©  Crustaceorum  in  depositis  Cam- 
brisis  et  Siluricis  Vestrogotise  Sueciae 
repertarum. 

In  Ofversigt.  Kongl.  Svenska  Vet.-Akad. 
Forhandl.,  1869,  No.  1,  p.  191. 

Remopleurides,  Triarthrus,  Phacops,  Trinu- 
cleus, Symphysurus,  Ogygia,  Niobe . Acidaspis, 
Cheirurus,  Cybele,  Dindymene,  Panderia,  Ag- 
nostus, Lichas i Leperditia,  Beyrichia,  Primitia, 
Trilobites  cenigma. 

Jemforelse  mellan  de  Siluriska  afla- 

gringarne  i Dalarne  ocb  i Yestergot- 
land. 

In  Ofversigt.  Kongl.  Svenska  Vet. -Acad. 
Forhandl.,  1871,  No.  3,  p.  339. 

Remopleurides,  Trinucleus,  Proetus,  Phacops, 
Chasmops,  Illcenus,  Nileus.  Beyrichia,  Primitia. 

Mere  mention  of  occurrence. 

Om  nagra  forsteningar  fran  Sveriges 

ocb  Norges  “Primordialzon.” 

In  Ofversigt  Kongl.  Svenska  Vet.-Akad.  For- 
handl., 1871,  No.  6. 

Paradoxides  kjerulfi,  pi.  16,  figs.  1-3. 

Anteckningar  om  den  Cambrisk- 

Siluriska  lagerserien  Jemtland. 

In  Geol.  Foreningens  Stockholm  Forhandl., 
vol.  1,  No.  3, 1872,  p.  34. 

Ofversigt  af  Nerikes  ofvergangsbild- 

ningar. 

In  Ofversigt  Kon  gl.  Svenska  V et.  - Akad . For- 
handl.,1875,  No.  5,  pi.  5;  Sveriges  Geologiska 
Undersokning  Ser.  C,  No.  21, 1875. 

Paradoxides,  Ellipsocephalus,  Leptoplastus 
n g.,  Beyrichia. 

Trilobiter  frau  Vestergotlands  An-  I 

drarurn  kalk. 

In  Geol.  Foreningens  Stockholm  Forhandl.,  j 
vol.  2, 1875,  p.  491. 


vogdes.1  LIST  OF 

Linnarsson  (J.  G.  O.)— Continued. 

En  egendomlig  Trilobitfauna  fran 

Jemtland. 

In  Geol.  Foreningens  Stockholm  Forhandl., 
vol.  2,  No.  12, 1875,  p.  491,  pi.  22,  figs.  1-5. 

IHeelloceji^alus  billing  si,  Triarthrus  jemt- 
landicus,  Remopleurides  microphthalmus,  Bohe- 
millaO ) denticulata. 

Tva  nya  Trilobiter  fran  Skanes 

alumskiffer. 

In  Geol.  Foreningens  Stockholm  Forhandl., 
vol.  2,  No.  12, 1875,  p.  498. 

Liostracus  (?)  superstes,  Cyclognathus  n.  g., 
O.  micropygus. 

Geologiska  iakttagelser  under  en 

resa  pa  Oland. 

In  Geol.  Foreningens  Stockholm  Forhandl., 
vol.  3,  No.  2, 1876,  p.  71. 

Om  faunan  i lagren  med  Paradoxides 

olandicus. 

In  SverigesGeologiska  Undersokning,  Ser.  C, 
No.  22, 1877,  2 pis. 

Paradoxides,  Ellipsocephalus , Gonocoryphe , 
Agnostus. 

Om  de  palseozoiskabildningarna  vid 

Humlenas. 

In  Sveriges  Geologiska  Undersokning,  Ser. 
C,  No.  28, 1878. 

On  the  Trilobites  of  the  Shineton 

shales. 

In  Geol.  Mag.,  new  series,  decade  2,  vol.  5, 
1878,  p.  188. 

Gonocoryphe,  Remopleurides. 

Om  faunan  i kalken  med  Gonocoryphe 

exsultans. 

In  Sveriges  Geologiska  Undersokning,  Ser. 
C,  No.  35, 1879,  3 pis. 

Paradoxides,  Liostracus,  Solenopleura,  Gono- 
coryphe, Agnostus. 

■ Ceratopygekalk  och  undre  grapto- 

litskiffer  p&  Falbygden,  i Vestergot- 
land. 

In  Geol.  Foreningens  Stockholm  Forhandl., 
vol.  4, 1879,  p.  269. 

Om  forsteningarne  i de  Svenska 

lagren  med  Peltura  och  Sphserophthal- 
mus. 

In  Geol.  Foreningens  Stockholm  Forhandl., 
vol.  5,  1880,  No.  4;  Sveriges  Geologiska  Under- 
sokning, Ser.  C,  No.  43,  1880. 

Peltura,  Sphcerophthalmus,  Anopocare,  Cte- 
nopyge  n.  g.,  Agnostus. 

Promemoria  lemnad  af  A.  G.  Na- 

thorst  for  resa  pa  Oland. 

In  Geol.  Foreningens  Stockholm  Forhandl., 
vol.  5,  No.  13, 188L 

De  undre  Paradoxides  lagren  vid 

Andrarum. 

In  Sveriges  Geologiska  Undersokning,  Ser. 
C,  No.  54,  1883,  4 pis. 


AUTHORS.  47 

Linne  (C.)  Olandska  och  Gotlandska 
resa.  Stockholm  och  Upsal,  1715. 

On  p.  147,  under  the  name  of  Entomolithus 
paradoxus,  there  is  in  this  work  a rough  wood- 
cut  of  the  pygidium  of  Asaphus  expansus  Linn. 

Wastgdta  resa  forrattad  ar  1746. 

Stockholm,  1747. 

On  pp.  87  and  88  of  this  work  there  are  some 
rough  wood-cuts  of  Trilobites,  probably  an 
Olenus  and  the  head  of  a Paradoxides. 

Museum  Tessinianum.  Holmise, 

1753,  p.  123,  pi.  3. 

Entomolithus,  pi.  3,  fig.  2 ( Galymene  tubercu- 
latus ):  E.  paradoxus,  pi.  3,  fig.  1 ( Paradoxides 
tessini). 

Skanska  resa.  Stockholm,  1757,  p. 

121. 

Petrificatet  Entomolithus  paradoxus 

beskrifed. 

In  Acta  Regiae  Acad.  Sci.  Holmiens.,  vol.  21, 
1759,  p.  19,  pi.  1,  figs.  1-4. 

Entomolithus  paradoxus,  pi.  1,  fig.  1 ( Olenus 
spinulosus) ; Entom.  paradoxus  8 cantliaridum, 
pi.  1,  fig.  4,  head  ( Olenus  gibbosus ) ; Entom.  No. 
3,  pi.  1,  fig.  3 ( Galymene  blumenbachii) ; Entom. 
No.  2,  pi.  1,  fig.  2 (Encrinurus  punctatus) . 

Systema  natures.  Ed.  12.  Vol.  3. 

Holmise,  1768,  p.  160. 

Entomolithus  paradoxus  a expansus  (Asa- 
phus expansus  Linn.).  E.  paradoxus  p canthari- 
dum  ( Olenus  gibbosus  "Wahl.),  E.  paradoxus  y 
pisiformis  (Agnostus pisiformis  Linn.). 

Littleton  (Charles).  On  a nondescript 
petrified  insect. 

In  Philos.  Trans.  Royal  Soc.  London,  vol.  46, 
No.  496,  1750,  p.  598,  pi.  1,  figs.  3-12,  pi.  2. 

Galymene  blumenbachii. 

Locke  (John).  On  Isotelus  maximus , 
found  near  Trebers,  in  Adams  County, 
Ohio. 

In  Second  Ann.  Rept.  Geol.  Survey  Ohio  (W. 
W.  Mather),  1838,  p.  247,  fig.  8. 

On  a new  species  of  Trilobite  of  very 

large  size. 

In  Trans.  Assoc.  Am.  Geol.  and  Naturalists, 
vol.  1, 1843,  p.  221,  plate. 

Isotelus  megistos  Locke. 

Dr.  John  Locke  has  herein  given  a new  name 
to  the  species  which  he  called  Isotelus  maxi- 
mus in  the  Second  Ohio  Report.  See,  also,  Am. 
Jour.  Sci.,  1st  series,  vol.  42, 1843,  p.  366, 1 pi. 

Notice  of  a new  Trilobite. 

In  Am.  Jour.  Sci.,  1st  series,  vol.  44, 1843,  p. 
346. 

Geraurus  crosotus. 

Supplementary  notice  of  the  Cerau- 

ru8  crosotus. 

In  Am.  Jour.  Sci.,  1st  series,  vol.  45,  1843,  p. 
223. 


A BIBLIOGRAPHY  OF  PALEOZOIC  CRUSTACEA.  [bull.  63. 


48 

liogan  (W.  E.)  Bronteus  canadensis. 

In  Kept.  Geol.  Survey  Canada,  1844,  p.  54,  2 
figs. 

On  the  tracks  of  an  animal  lately 

found  in  the  Potsdam  sandstone. 

In  Canadian  Naturalist,  vol.  5, 1860,  p.  279. 

Lossen  (K.  A.)  Ueber  Cryphceus  rotundi- 
frons  aus  dem  zorger  Schiefer  des 
siidlichen  Unterharzes. 

In  Zeitsebr.  Deutsch.xgeol.  Gesell.,  vol.  31, 
1879,  p.  215. 

Cryphceus. 

Loven  (S.  L.)  On  Calymene  clavifrons 
and  C.  ovata. 

InOfversigtKongl.  Svenska  Vet.-Akad.  For- 
handl.,1845,  p.  63. 

Svenska  Trilobiter. 

InOfversigt  Kongl.  Svenska  Vet.-Akad.  For- 
handl.,  1845,  pp.  46, 104,  pis.  1,  2. 

Trinucleus,  Proetus,  Metopias,  Lichas,  Cerate- 
ru*,  Cybele  n.  g. 

Lungren  (B.)  Om  den  vid  Rams&sa  och 
Ofveredskloster  i Skane  forekommande 
sandst$nens  alder. 

In  Acta  Univ.  Lundensis,  1874. 

Leperditia. 

MacLeay  ( W.  S.  ) Observations  on 
Trilobites,  founded  on  a comparison  of 
their  structure  and  that  of  living  Crus- 
tacea. 

In  R.  I.  Murchison.  ‘ ‘ The  Silurian  system , ’ ’ 
London,  1839,  p.  666;  Annals  Mag.  Nat.  Hist., 
1st  series,  London,  vol.  4,  1839,  p.  16. 

The  author  compares  them  with  Apus  and 
other  Aspidophora,  animals  which,  in  his 
opinion,  of  all  the  Entomostraca,  appear  to  come 
nearest  to  the  Trilobita. 

McCoy  (Frederick).  On  Entomoconchus 

8Conli. 

In  Jour.  Geol.  Soc.  Dublin,  vol.  11, 1839,  p.  91, 
pi.  5,  figs,  a,  c. 

Entomoconchus  n.  g. 

A synopsis  of  the  characters  of  the 

Carboniferous  limestone  fossils  of  Ire- 
land. Dublin,  1844,  29  pis. 

The  title-page  bears  no  author’s  name.  The 
book  shows  that  it  was  prepared  by  Frederick 
McCoy,  under  the  direction  of  Richard  Griffith, 
the  collector,  in  whose  cabinet  all  the  speciae 
were  contained. 

Phillipsia,  OriJJithides,  Calymene , Dithyro- 
caris,  Entomoconchus , Cytherina,  Bairdia  n.  g., 
Cythere,  Daphma. 

A synopsis  of  the  Silurian  fossils  of 

Ireland,  collected  from  the  several  dis- 
tricts by  Richard  Griffith,  F.  G.  S. 
The  whole  being  named,  and  the  new 


McCoy  (Frederick) — Continued, 
species  drawn  and  described,  by  Fred- 
erick McCoy.  Dublin,  1846,  5 pis. 

Harpes,  Remopleurides,  Forbesia  n.  g.,  Pha - 
cops,  Portlockia  n.  g.,  Calymene,  Homalonotus, 
Lichas,  Trinucleus,  Ampyx,  Ogygia,  Isotelus, 
lllcenus,  Acidaspis,  Cheirurus,  Sphcerexochus, 
Otarion,  Encrinurus,  Bronteus,  Trinodus  u.  g., 
Tiresias  n.  g.,  Beyrichia  n.  g.,  Cythere,  Battus. 

A notice  of  the  new  genera  described  by 
Frederick  McCoy  is  given  in  the  Ray  Society’s 
edition  of  Burmeister’s  “ Organization  of  Trilo- 
bites. Supplementary  appendix,”  p.  123. 

The  generic  name  Tiresias  was  used  in  1845 
for  a genus  of  the  Coleoptera,  and  that  of 
Forbesia  for  one  of  the  Polypi  in  1845.  Trinodus 
was  used  in  1846  for  a genus  of  the  Coleoptera. 

On  the  fossil  botany  and  zoology  of 

the  rocks  associated  with  the  coal  of 
Australia. 

In  Annals  Mag.  Nat.  Hist.,  1st  series,  Lon- 
don, vol.  20,  1847,  p.  226,  plato. 

Phillipsia,  Brachymetopus  n.  g.,  Cythere, 
Bairdia. 

On  the  classification  of  some  British 

fossil  Crustacea,  with  notices  of  new 
forms  in  the  University  collection  at 
Cambridge. 

In  Annals  Mag.  Nat.  Hist.,  2d  series,  Lon- 
don, vol.  4,  1849. 

Asaphime:  1.  Phacops,  2.  Calymene , 3.  Tri- 
merocephalus  n.  g.,  4.  Asaphus  (subgenera,  Iso- 
letus,  Basilicus),  5.  lllcenus  (subgenera,  lllcenus, 
Bumastus,  Dysplanus),  6.  Forbesia,  7.  Phil- 
lipsia. Paradoxinse : 1.  Paradoxides  (subgenus, 
Olenus),  2.  Ceraurus,3.  Cryphceus,  A Sphcerexo- 
chus, 5.  Acidaspis,  6.  Staurocephalus,  7.  Remo- 
pleurides,  8.  Zethus.  Ogyginm : 1.  Trinucleus 
(subgenus,  Tetrapsellium)  ',  2.  Tretaspis  n.  g.,  3. 
Ampyx,  4.  Ogygia,  5.  Bronteus,  6.  Lichas  (sub- 
genera,  Trochurus,  Acanthopyge).  Harpedinse : 
1.  Harpes,  2.  Harpidella  n.  g.,  3 Amphion.  Ag- 
nostinse : 1.  Trinodus,  2.  Agnostus,  Chasmopsxt. 
g.,  Oriffi,thides,  Barrandia  n.  g.,  Ceratiocaris 
n.  g.,  Cytheropsis  n.  g.,  Pterygotus. 

Partly  republished  in  the  author’s  “Contri- 
butions to  British  Palaeontology,  etc.,”  London, 
1854. 

On  the  supposed  fish  remains  figured' 

on  plate  4 of  “ The  Silurian  system. 

In  Quart.  Jour.  Geol.  Soc.  London,  vol.  9, 
1853,  p.  13. 

A synopsis  of  the  classification  of 

the  British  Palaeozoic  rocks,  by  Adam 
Sedgwick ; with  a systematic  descrip- 
tion of  the  British  Palaeozoic  fossils  in 
the  Geological  Museum  of  Cambridge, 
by  Frederick  McCoy,  with  figures  of  the 
new  and  imperfectly  known  species. 
London  and  Cambridge,  1855,  25  pis. 
Pt.  2.  Palaeontology. 


V0GDES.J 


LIST  OF  AUTHORS. 


49 


McCoy  (Frederick) — Continued. 

Fasciculus  1.  Radiata  and  Articulata.  Lon- 
don, 1851. 

Fasciculus  2.  Lower  and  Middle  Palaeozoic 
Mollusca.  London,  1852. 

Fasciculus  3.  Upper  Palaeozoic  Mollusca  and 
fish.  London  and  Cambridge,  1855. 

Harpes,  Foroesia , Phacops , Odontochile,  Ohas- 
mops,  Portlockia,  Calymene,  Homalonotus , Tro- 
churus,  Lichas,  Trinucleus,  Harpidella,  Tretas -- 
pis,  Ampyx,  Isotelus,  Ogygia,  Barrandia,  Ad, 
daspis,  Ceraurus,  Eccoptochile,  Staurocephalus- 
Encrinurus,  Zethus,  Illcenus,  Dysplanus,  Bi 
plorhina,  Agnostus,  Acanthopyge,  Eurypterus, 
Pterygotus,  Leptocheles  n.  g.,  Ceratiocaris,  Bey- 
richia,  Cytheropsis,  Trinodus. 

Contributions  to  British  palaeon- 
tology, or  first  description  of  360  species 
and  several  genera  of  fossil  Radiata, 
Articulata,  Mollusca  and  Pisces  from 
the  Tertiary,  Cretaceous,  Oolitic  and 
Palaeozoic  strata  of  Great  Britain.  Re- 
published from  the  Annals  Mag.  Nat. 
Hist.  Cambridge,  1854. 

For  a list  of  the  genera  of  fossil  Crustacea, 
see  entries  under  McCoy  (Frederick),  Annals 
Mag.  Nat.  Hist.,  2d  series,  London,  vol.  4, 1849. 

Geological  Survey  of  Victoria.  Pro- 

dromus  of  the  palaeontology  of  Vic- 
toria, or  figures  and  descriptions  of 
Victorian  organic  remains,  decade  3. 
Melbourne  and  London,  1875,  pis.  22, 23. 

Phacops  ( Odontochile ) caudatus , P.  ( Port- 
lockia) fecundus,  Forbesia  euryseps  McCoy, 
Licha8  australis  McCoy,  Homalonotus  harri- 
soni  McCoy. 

Mantell  ( G. ) Medals  of  creation,  or 
first  lessons  in  geology  and  the  study 
of  organic  remains.  2 vols.  London, 
1854. 

Marcou  (Jules).  On  the  Primordial 
fauna  and  the  Taconic  system,  by 
Joachim  Barrande ; with  additional 
notes  by  Jules  Marcou. 

In  Proc.  Boston  Soc.  Nat.  Hist.,  vol.  7,  1861. 
p.  369. 

Notice  sur  les  gisements  des  lentilles 

trilobitif&res  taconique  de  la  Pointe 
LAvis  ou  Canada. 

In  Bull.  Soc.  G6ol.  France,  2d  series,  vol.  21, 

1864,  p.  236. 

Marr  (J.  E.)  On  some  well-defined  life 
zones  in  the  lower  part  of  the  Silurian 
(Sedgwick)  of  the  Lake  District. 

In  Quart.  Jour.  Geol.  Soc.  London,  vol.  34, 
1878,  p.  871. 

Appendix.  On  some  species  of  Phacops , p. 

884. 


Marr  (J.  E.) — Continued. 

and  Nicholson  <H.  A.)  The  Stock- 

dale  shales. 

In  Quart.  Jour.  Geol.  Soc.  London,  vol.  44, 
1888,  p.  654,  pi.  16. 

Harpes,  Proctus,  Phacops , Ampyx,  Acidaspis, 
Oheiruru8. 

Martin  (D.  S.)  A new  Eurypterid  from 
the  Catskiil  group. 

In  Trans.  New  York  Acad.  Sci.,  vol.  2,  1882, 

p.8. 

This  notice  was  based  upon  a cast  of  Sty- 
lonurus  excelsior  Hall,  obtained  from  the  Mu- 
seum of  Natural  History,  Albany,  New  York. 
Martin  (W.)  Petrificata  Derbiensia:  a 
description  of  petrifactions  collected  in 
Derbyshire.  Wigan,  1809, 4to,  53  pis. 

Entomolithue  oniscites  (derbiensis) , pi.  45,  figs. 
1-3;  Entomolithus  monoculites ? ( lunatus ),  pi. 
45,  fig.  4;  Entom.  paradoxus,  from  Dudley,  pi. 
45.  fig.  3;  also  pi.  45a;,  fig.  3. 

These  fossils  have  been  referred  to  the  fol- 
lowing modern  genera:  Phillip sia  derbiensis,  pi. 
45,  figs.  1-3,  and  pi.  45a;,  fig.  3 ; Belinurus,  pi. 
45,  fig.  4,  Calymene  blumenbachi,  pi.  45,  fig.  3. 

Matthew  (G.  F.)  Illustrations  of  the 
fauna  of  the  St.  John  group.  No.  1. 
The  Paradoxides;  their  history. 

In  Trans.  Royal  Soc.  Canada,  vol.  1, 1882,  Sec. 
4,  p.  87,  pi.  9. 

Paradoxides  etemenicus  Matt.,  Par.  acadicus 
Matt.,  P.  lamellatus  Hartt. 

Illustrations  of  the  fauna  of  the  St. 

John  group.  No.  1.  The  Paradoxides 
(supplementary  section  describing  the 
parts). 

In  Trans.  Royal  Soc.  Canada,  vol.  1, 1882,  Sec. 
4,  p.  271,  pi.  10. 

Illustrations  of  the  fauna  of  the  St. 

John  group,  continued:  On  the  Cono- 
coryphea , with  further  remarks  on  Para- 
doxides. 

In  Trans.  Royal  Soc.  Canada,  vol.  2, 1884,  Sec. 
4,  p.  99,  pl.l. 

Paradoxides,  Otenocephalus,  Oonocoryphe. 

In  his  explanation  of  the  plate,  fig.  6,  the  au- 
thor uses  a now  subgenus,  Otenocephalus  ( Har - 
tella)  matthewi,  and  also  for  fig.  22,  Oonocoryphe 
(Bailiella)  baileyi. 

An  outline  of  recent  discoveries  in 

the  St.  John  group. 

In  Bull.  New  Brunswick  Nat.  Hist.  Soc.,  No 
4,  1884. 

Illustrations  of  the  fauna  of  the  St. 

John  group.  No.  3.  Descriptions  of 
new  genera  and  species  (including  a 
description  of  a new  species  of  Soleno- 
pleura,  by  J.  F.  Whiteaves). 

In  Trans.  Royal  Soc.  Canada,  vol.  3, 1885,  p.  29, 
3 pis. 


BULL.  03 1 


A BIBLIOGRAPHY  OF  PALEOZOIC  CRUSTACEA.  [bull.  63. 


50 

Matthew  (G.F.)— Continued. 

Lepidittan.  g.,  Lepidillavc.  g.,  Beyrichia,  Hip- 
ponicharion  n.  g.,  Beyrichona  n.  g.,  Primitia , 
Agnostics,  Hicrodiscus,  Agraulos,  Solenopleurcc, 
Paradoxides. 

On  the  probable  occurrence  of  the 

great  Welsh  Paradoxides , P.  davidis,  in 
America. 

In  Am.  Jour.  Sci.,  3d  series,  vol.  30, 1885,  p.  72; 
Nature,  vol.  32, 1885,  p.  358. 

Abstract  of  a paper  on  the  Cambrian 

fauna  of  Cape  Breton  and  Newfound- 
land. 

In  Canadian  Record  Sci.,  vol.  2, 1886,  p.  255. 

Note  on  the  occurrence  of  Olenellus? 

kjerulfi  in  America. 

In  Am.  Jour.  Sci.,  3d  series,  vol.  31, 1886,  p.  472. 

On  the  Cambrian  fauna  of  Cape  Bre- 
ton and  Newfoundland. 

In  Trans.  Royal  Soc.  Canada,  vol.  2,  1886,  p. 

147. 

Agraulos,  Selenopleura. 

Illustrations  of  the  fauna  of  the  St. 

John  “group.  No.  4.  On  the  smaller 
eyedTrilobites  of  Division  1,  with  a few 
remarks  on  the  species  of  the  higher 
division  of  the  group. 

In  Canadian  Record  Sci.,  vol.  2,  No.  6, 1887,  p. 
357. 

On  the  kin  of  Paradoxides  ( Olenellus  ?) 

lcjerulji. 

In  Am.  Jour.  Sci.,  3d  series,  vol.  33,  1887,  p. 
390. 

The  great  Acadian  Paradoxides. 

In  Am.  Jour.  Sci.,  3d  series,  vol.  33,  1887,  p. 
388. 

Paradoxides  regina  Matt. 

Illustrations  of  the  fauna  of  the  St. 

John  group.  No.  4.  Part  1.  Descrip- 
tion of  a new  species  of  Paradoxides  ( P. 
regina ).  Part  2.  The  smaller  Trilo- 
bites  with  eyes  ( Ptychoparidce  and  El- 
lipsocephalidce ). 

In  Trans.  Royal  Soc.  Canada,  vol.  5, 1887,  p. 
115,  3 pis. 

Paradoxides,  Liostracus,  Strenuella  n.  sub- 
gen., Ptychoparia,  Solenopleurcc,  Agraulos,  Ellip- 
socephalus. 

Maurer  (F.)  Palaontologische  Studien 
im  Gebiet  des  rheinischen  Devon.  Die 
Fauna  des  Rotheisenstein  der  Grube 
Haina. 

In  Neues  Jahrbuch  fur  Mineral.,  1875,  p.  596, 

pi.  14. 

Phcccops  latifrons,  Cypliaspis  ceratophtlial- 

mus. 


Maurer  (F.)— Continued. 

Palaontologische  Studien  im  Gebiet 

des  rheinischen  Devon.  Die  Thon- ' 
schiefer  des  Ruppbachthales  bei  Diez. 

In  Neues  Jahrbuch  fur  Mineral.,  1876,  p.  8&8, 
pi.  14. 

Phacops,  Acidaspis,  Brontcus. 

Die  Fauna  der  Kalke  von  Wald- 

girmes  bei  Giessen. 

In  Abhandl.  grossh.-hess.  geol.  Landesanstalt 
zu  Darmstadt,  vol.  1,  pt.  2, 1885,  atlas  of  11  pis. 

Harpes,  Phacops,  Proetus,  Gyphaspis,  Oheiru- 
rus,  Bronteus,  Primitia,  Orozoe. 

Meek  (F.  B.)  Note  on  Belinurus  dance , 
from  the  Illinois  Coal  Measures. 

In  Am.  Jour.  Sci.,  2d  series,  vol.  43,  1867,  p. 
257  ; Geol.  Survey  Illinois,  vol.  2,  p.  395. 

Note  on  a new  genus  of  fossil  Crus- 
tacea. 

In  Am.  Jour.  Sci.,  2d  series,  vol.  43,  1867,  p. 
394  ; Geol.  Survey  Illinois,  vol.  3,  p.  547. 

Euproops  (n.  g.). 

Descriptions  of  fossils  collected  by 

the  U.  S.  Geological  Survey,  under 
charge  of  Clarence  King. 

In  Proc.  Acad.  Nat.  Sci.  Phila.,  vol.  22,  1870, 
p.  56. 

Republished  and  illustrated  in  Rept.  U.  S. 
Geol.  Expl.,  40th  Parallel,  vol.  4,  pt.  1,  pp. 
1-197,  pis.  1-17. 

Paradoxides , Conocoryphe  ( Conocephalites ), 
Olenics. 

Descriptions  of  new  species  of  in-. 

vertebrate  fossils  from  the  Carbonifer- 
ous and  Devonian  rocks  of  Ohio. 

In  Proc.  Acad.  Nat.  Sci.  Phila.,  vol.  23, 1§71, 
p.  57. 

Republished  and  figured  in  “ Palseontology 
of  Ohio,”  vol.  1, 1873,  p.  233, 23  pis. 

Proetus  planimarginatus,  Dalmanites  ohio- 
ensis. 

Descriptions  of  new  Western  Palaeo-  , 

zoic  fossils,  mainly  from  the  Cincin- 
nati group  of  the  Lower  Silurian  seriea 
of  Ohio. 

In  Proc.  Acad.  Nat.  Sci.  Phila.,  vol.  23, 1871,  p* 
308. 

Redescribed  and  illustrated  in  “Palaeontol- 
ogy of  Ohio,”  vol.  2, 1875. 

Gythere,  Ceratiocaris  ( Colpocaris ),  Archceoca- 
ris,  Solenocaris,  Colpocaris.  (Not  Solenocarie 
Young,  1868.) 

List  of  Carboniferous  fossils  from 

West  Virginia,  with  descriptions  of 
new  species. 

In  Appendix  B,  Rept.  of  Regents  of  West 
Virginia  Univ.,  1870,  Wheeling,  1871,  p.  68. 

Phillipsia  stevensoni  Meek. 

Final  report  of  the  U.  S.  Geological, 

Survey  of  Nebraska  and  portions  of  the 


VOGDES.] 


LIST  OF  AUTHORS.  51 


Meek  (F.  B.)— Continued, 
adjacent  Territories,  by  F.  V.  Hayden, 
etc.  Report  on  the  paleontology  of 
eastern  Nebraska,  with  some  remarks 
on  the  Carboniferous  rock  of  that 
district  by  F.  B.  Meek.  Washington, 
1871,  p.  83,  11  pis.  ( Two  editions : 
first  in  8vo,  second  in  4to.) 

Phillipsia,  Gythere. 

Genus  Archceocaris. 

In  Proc.  Acad.  Nat.  Sci.  Phila.,  vol.  24,  1872, 
p.  325. 

Description  of  new  species  of  fossils 

from  Cincinnati  group,  Ohio. 

In  Am.  Jour.  Sci.,  3d  series,  vol.  3, 1873,  p.  423. 

Proetus,  Dalmanites. 

Preliminary  palaeontological  report, 

consisting  of  list  and  descriptions  of 
fossils,  with  remarks  on  the  age  of  tbe 
rocks  in  which  they  are  found,  etc. 

In  Sixth  Ann.  Kept.  U.  S.  Geol.  Survey  Terri- 
tories, embracing  portions  of  Montana,  Idaho, 
"Wyoming,  and  Utah,  etc.  F.  V.  Hayden, 
Washington,  1873,  p.431. 

Conocoryphe  (Ptychoparia) , Bathyurus,  Ba- 

„ thyurella  (Asaphiscus)  n.  sg.,  Asaphus,  (Megal- 
aspis),  Agnostus. 

Report  of  the  Geological  Survey  of 

Ohio.  Vol.  1.  Geology  and  palaeon- 
tology. Pt.2.  Palaeontology.  Descrip- 
tions of  invertebrate  fossils  of  the  Silu- 
rian and  Devonian  systems,  by  F.  B. 
Meek. 

Columbus,  1873.  pp.  1-243,  pis.  1-23. 

Proetus,  Dalmanites , Calymene,  Asajjhus 
( Dotelus ),  Acidaspis,  Ceraurus,  Illcenus  (Bu- 
mastu8),  Gythere , Leperditia. 

Descriptions  of  Olenus  ( Olenellus ) 

gilberti  and  Olenus  (Olenellus)  hoivelli. 

In  Kept.  Geog.  and  Geol.  Expl.  Surveys  West 
100th  Her.,  vol.  3,  Washington,  1875,  p.  182. 

A report  on  some  of  the  invertebrate 

fossils  of  the  Waverly  group  and  Coal 
Measures  of  Ohio. 

In  Kept.  Geol.  Survey  Ohio.  Vol.  2.  Geology 
and  Palaeontology.  Pt.  2.  1875,  pp.  269-347,  pis. 
10-20. 

Phillipsia , Griffithides,  Geratiocaris  ( Oolpo - 
caris),  Geratiocaris  ( Solenocaris ),  Archceocaris , 

Oolpocaris,  Solenocaris. 

Palaeontology. 

In  U.  S.  Geol.  Expl.  40th  Parallel,  vol.  4,  pt.  1, 
1877,  pp.  1-197,  pis.  1-17. 

Paradoxules , Gonocoryphe  ( Ptychoparia ), 
Proetus,  Dalmanites. 

and  Hayden  (F.  V.)  Descriptions 

of  new  Lower  Silurian,  Jurassic,  Creta- 
ceous, aud  Tertiary  fossils  collected  in 


Meek  (F.  B.)  and  Hayden  (F.  V.)— Con- 
tinued. 

Nebraska  by  the  exploring  expedition 
under  the  command  of  Capt.  W.  F. 
Raynolds,  U.  S.  Top.  Eng.,  with  re- 
marks on  the  rocks  from  which  they 
were  obtained. 

In  Proc.  Acad.  Nat.  Sci.  Phila.,  vol.  13,  1862, 
p.  415. 

Arionellus,  Arionellus  ( Grepicephalus ) oweni. 

Palaeontology  of  the  Upper  Mis- 
souri. A report  upon  collections  made 
principally  by  the  expeditious  under 
command  of  Lieut.  G.  K.  Warren,  U.  S. 
Top.  Eng.,  in  1855-56.  Invertebrates. 
Pt.  1. 

In  Smithsonian  Contrib.,  No.  172,  Washing- 
ton, 1864,  5 pis. 

Paradoxides,  Agraulos , Agraulos  oweni  M. 
& H. 

and  Worthen  (A.  H.)  Notice  of 

some  new  types  of  organic  remains  from 
the  Coal  Measures  of  Illinois. 

In  Proc.  Acad.  Nat.  Sci.  Phila.,  vol.  17,  1865, 
p.  41. 

Acanthotelson  n.  g.,  Belinurus , Anthrapalce- 
mon,  Palceocaris  n.  g. 

Contributions  to  the  palaeou- 

- tology  of  Illinois  and  other  Western 
States. 

In  Proc.  Acad.  Nat.  Sci.  Phila.,  vol.  17,  1865, 
p.  245. 

Proetus,  Phillipsia,  Griffithides,  Dalmania, 
Lichas. 

Descriptions  of  invertebrates 

from  the  Carboniferous  system. 

In  Geol.  Survey  Illinois,  vol.  2, 1866,  p.  145,  pis. 
14-20,  23-32. 

Belinurus,  Acanthotelson , Palceocaris,  An- 
thrapalcemon. 

— — Preliminary  notice  of  a scor- 
pion, a Eurypterus,  and  other  fossils 
from  the  Coal  Measures  of  Illinois. 

In  Am.  Jour.  Sci.,  2d  series,  vol.  46, 1868,  p.  19. 
Republished  and  illustrated  in  “Geol.  Survey 
Illinois,”  vol.  3,  p.  560. 

Palaeontology. 

In  Geol.  Survey  Illinois,  vol.  3,  1868,  pp.  291- 
565,  pis.  1-20. 

Proetus,  Phacops,  Dalmanites  ( Odonocepha - 
lus),  Lichas,  Acidaspis,  Illcenus,  Ceratiocaris, 
Euproops , Palceocaris,  Euryplerus  (Anthrapa- 
Icemon),  Acanthotelson. 

Descriptions  of  a now  species 

and  genera  of  fossils  from  tlio  Palaeo- 
zoic rocks  of  the  Western  States. 

In  Proc.  Acad.  Nat.  Sci.  Phila.,  2d  series,  vol. 

| 14,  1870,  p.  22. 


52 


A BIBLIOGRAPHY  OF  PALEOZOIC  CRUSTACEA. 


[BULL.  63. 


Meek  (F.  B.)  and  Wortfcen  (A.  H.)— 
Continued. 

Phillip  si  a tuberculata  M.  & W.,  Phillipsia 
(Griffithides)  bufo  M.  & W.,  Asaphus  (Isotelus) 
vigilant  M.  & W.,  Ulcenus  ( Bumastus ) graf- 
tonensis  M.  & "W.,  Dithyrocaris  carbonarius 
M.&  W. 

Descriptions  of  invertebrates 

from  tbe  Carboniferous  system. 

In  Geol.  Survey  Illinois,  vol.  5,  1873,  pp.  323- 
619,  pis.  1-32. 

Phillipsia  ( Griffithides ) portlocki,  Phillipsia 
( Griffithides ) bufo,  Phillipsia  (Griffithides)  sci- 
tula,  Dithyocari8  carbonarius. 

Description  of  tbe  inverte- 
brates. 

In  Geol.  Survey  Illinois,  vol.  6,  1875,  pp.  489- 
532,  pis.  23-33. 

Lichas,  Asaphus  (Isotelus),  Sphcerexochus, 
Ulcenus  (Bumastus). 

Meneghini  (Giuseppe).  Nuovi  fossiii  si- 
luriani  di  Sardegna. 

In  Atti  reale  Accad.  Lincei,  Roma,  1880, 1 pi. 

Dalmanites,  Lamarmorce. 

Posizione  relativa  dei  varii  piani 

siluriani  dell’  Iglesiente  in  Sardegna. 

In  Pfoc.  verb.  Soc.  Toscana  Sci.  Nat.,  1881,  p. 
258. 

Paradoxides,  Trinucleus , Dalmanites , Conoce- 
phalites. 

Fauna  Cambriana  dell’  Iglesiente  in 

Sardegna. 

In  Proc.  verb.  Soc.  Toscana  Sci.  Nat.,  1881,  p. 
158. 

Paradoxides,  Olenus,  Conocephalites. 

Nuovi  Trilobiti  di  Sardegna. 

In  Proc.  verb.  Soc.  Toscana  Sci.  Nat.,  1881,  p. 

200. 

Paradoxides,  Conocephalites. 

Note  alia  fauna  Cambriana  dell’ 

Iglesiente. 

In  Proc.  verb.  Soc.  Toscana  Sci.  Nat.,  1882, 
p.7. 

Olenus,  Anomocare,  Conocephalites,  Platypelm 
tis. 

Nuovi  fossiii  Cambrian i di  Sardegna. 

In  Proc.  verb.  Soc.  Toscana  Sci.  Nat.,  1884, 
p.  56. 

Conocephalites,  Anomocare. 

Palaeontologia  dell’  Iglesiente  in 

Sardegna.  Fauna  Cambriana  trilo- 
biti. 

In  Mem.  R.  Com.  Geol.  Italia,  vol.  3, 1888,  pt. 
2,  49  pp.,  7 pis. 

Paradoxides,  Olenus,  Anomocare,  Conocepham 
lites,  Asaphus  (Platypeltis),  Conocoryphc. 

Meyer  (H.  von).  Beitriige  zur  Petre- 
facten-Kunde. 

In  Nova  Acta  Acad.  Leop.  Carol.,  vol.  15, 1831, 
p.  57,  pi.  56,  fig.  13.  See,  also,  Neues  Jabrbuch 
fur  Mineral.,  1833,  p.  481. 

Calymene  cequalis  Meyer. 


Meyer  (H.  von)  and  Munster  (G.  G.  zu). 
Beitrage  zur  Petrefacten-Kunde.  Bay- 
reuth, 1840.,  pt.  3,  pi.  5. 

Calymene  variolaris,  C.  intermedia,  C.  Icevis, 

C.  sternbergi,  C.  propinqua,  O.  articulata , Asa- 
phus? caudori,  A.  pusillus,  A.?  brevis,  A. 
grandis,  Ulcenus  perovalisf,  Paradoxides  brevi-  . 
mucronatus,  Brontes  radiatus,  B.  costatus,  B. 
subradiatus,  Bumastus  Jr ankonicus,  B.  planus, 
Harpes  speciosus,  Trinucleus  gracilis,  T.tvil- 
kensii,  T.  ellipticus,  T.  nelsoni,  T.  ? otarion,  T.  ? 
gibbosus,  Agnostus  pisiformis. 

Beitrage  zu  Petrefacten-Kunde. 

Bayreuth,  1842,  pt.  5,  p.  112.  Nachtrag 
zu  den  Yersteinerungen  des  Ueber-  ' 
gangs-Kalkes  mit  Clymenien  von  Ober- 
franken  vom  Herausgeber. 

Calymene  marginata,  pi.  10,  fig.  6 ; C.furcata, 
Asaphus  dubius,  Ellipsocephalus  hoffi,  Otarion  ' 
elegans,  Harpes,  Trinucleus?  Icevis,  T.  inter me- 
dius,  T.  nilsoni. 

Squaliden-Reste  aus  dem  Posidono- 

myen-Schiefer  des  Oberharzes  bei  Ober- 
Schulenburg. 

In  Danker  and  von  Meyer  “ Palaeont.,  ” vol. 

3,  Cassel,  1854,  p.  53. 

Harpes,  Proetus,  Phacops,  Lichas,  Cheirurus. 

See,  also,  Jordon  (H.)  and  Meyer  (H.  von).  - \ 

Mickleborough  ( John ).  Locomotory 
appendages  of  Trilobites. 

In  Jour.  Cincinnati  Soc.  Nat.  Hist.,  vol.  6, 1883, 
p.  200,  figs.  1-3.  Noticed:  Am.  Jour.  Sci.,  3d 
series,  vol.  27,  1884,  p.409;  Geol.  Mag.,  n.  s.,  de- 
cade 3,  vol.  1,  London,  1884,  p.  80. 

Asaphus  megistos  Locke. 

Miller  (S.  A ) Monograph  of  the  Crusta- 
cea of  the  Cincinnati  group. 

In  Cincinnati  Quart.  Jour.  Sci.,  vol.  1, 1874,  p. 
115. 

Triarthrus,  Proetus,  Dalmanites,  Calymene^ 
Lichas,  Trinucleus,  Asaphus,  Isotelus,  Acid- 
aspis,  Ceraurus,  Beyrichia,  Leper ditia,  Cy there.' 

The  author,  in  his  classification  aud  generic 
descriptions,  has  generally  followed  McCoy 
(“Brit.  Palaeozoic  Bocks,”  1855).  He  gives  a 
description  of  the  different  fossil  Crustacea  oc- 
curring in  the  Cincinnati  group,  and  figures 
Leperditia  byrnesi  Miller,  and  a wood-cut  rep- 
resenting the  tracks  of  an  Asaphus  (?). 

[No  title. — Description  of  new  spe- 
cies of  Palaeozoic  Entomostraca.] 

In  Cincinnati  Quart.  Jour.  Sci.,  vol.  1, 1874,  p. 

232. 

Beyrichia  duryi,  B.  striato-marginatus,  B. 
chambersi. 

Some  new  species  of  fossils  from  the 

Cincinnati  group,  and  remarks  upon 
some  described  forms. 

In  Cincinnati  Quart.  Jour.  Sci.,  vqI,  2,  1875, 
p.  349,  figures. 

Acidaspis,  Beyrichia,  Leperditia. 


vOgdes.] 


LIST  OF  AUTHORS. 


53 


Miller  (S.  A. )— Continued. 

The  American  Palaeozoic  fossils.  A 

catalogue  of  the  genera  and  species, 
with  names  of  authors,  dates,  places  of 
publication,  group  of  rocks  in  which 
found,  and  the  etymology  and  significa- 
tion of  the  words,  etc.  Cincinnati, 
1877.  Also  a 2d  ed.,  with  supplement. 

Description  of  a new  genus  and 

eleven  new  species  of  fossils,  with  re- 
marks upon  others  well  known,  from 
the  Cincinnati  group. 

In  Jour.  Cincinnati  Soc.  Hat.  Hist.,  vol.  1, 
1878-79,  p.  100,  pi.  3. 

Lichas  harrisi,  Cythcre  irregularis. 

Description  of  two  new  species  from 

the  Niagara  group,  and  five  from  the 
Keokuk  group. 

In  Jour.  Cincinnati  Soc.  Hat.  Hist.,  vol.  2, 
1879,  p.  254,  pi.  15. 

Encrinurus  egani. 

Description  of  new  species  of  fossils. 

In  Jour.  Cincinnati  Soc.  Hat.  Hist.,  vol.  4, 

1881,  p.  259,  pi.  G. 

Leperditia  coecigena. 

Description  of  three  new  species, 

and  remarks  upon  others. 

In  Jour.  Cincinnati  Soc.  Hat.  Hist.,  vol.  5, 

1882,  p.  116,  pi.  5. 

Calymene  callicephala  Green. 

Milne-Edwards  (H.)  Sur  les  affinitds 
des  Trilobites. 

In  Institut  de  France,  Acad.  Royale  Sci., 
vol.  1,  1827,  p.  254. 

Trilobites  dans  Lamarck's  “Histoire 

natnrelle  des  animaux  sans  vertkbres.” 
Vol.  5.  Paris,  1838,  p.  220. 

Paradoxides,  Ellipsocephalus,  Conocephalus , 
Triarthrus , Calymene , Ampyx,  Asaphus,  Ogygia, 
Otarion,  Agnostus,  Ceraurus,  Oypridina  n.  g. 

Histoire  naturelle  des  Crustac^s, 

comprenant  l'anatomie,  la  physiologie 
et  la  classification  de  ces  animaux. 
[3  vols.,  with  atlas  of  plates.]  Paris, 
1834-’40. 

The  Trilobites  are  described  in  vol.  3,  pp. 
285-346,  in  the  following  order:  Nileus,  Am- 
pyx, Isotelus,  Asaphus , Ilomalonotus,  Calymene, 
Pleuracanthe  n.  g.  (referred  by  author  to  Dal- 
manites),  Trinucleus,  Otarion,  Ogygia,  Para- 
doxides, Peltura  n.  g.  (the  first  species  cited 
by  the  author  under  this  new  genus  was: 
Peltura  scaraboeoides  Wablenburg;  the  second, 
Peltura  bucklandi  Milne-Edwards,  is  a species 
of  the  genus  Lichas),  Agnostus,  Eurypterus. 
Classifies  64  species  under  13  genera. 

■ Report  on  the  palaeontological  re- 

searches of  M.  Marie  Ronault  in  Brit- 
tany and  Anjou. 


Milne-Edwards  (H.) — Continued. 

In  Coraptes  Rendus  Acad.  Sci.  Paris,  1847, vol. 
24,  p.  593;  Bull.  Soc.  G6ol.  France,  vol.  4,  1847, 
p.  309;  Quart.  Jour.  Geol.  Soc.  London,  vol.  4, 
1848,  pt.  2,  Miscellaneous,  p.  35. 

Trimccleus,  Calymene,  Phacops , Polyeres  n. 
g.,  Prionocheilus,  Cheirurus,  Nileus,  Ogygia, 
I llcenus. 

Structure  des  Trilobites. 

In  Annales  Sci.  Hat.,  vol.  12,  1881, 33  pp.,  pis. 
1-3. 

A review  of  C.  D.  Walcott’s  “Organization 
of  Trilobites.” 

Acidaspis,  Calymene,  Ceraurus,  Trinucleus, 
Asaphus,  Eurypterus. 

Mitchell  (John).  On  some  new  Trilo- 
bites from  Bowning,  N.  S.  W. 

In  Proc.  Linnean  Soc.  Hew  South  Wales,  2d 
series,  vol.  2,  1887,  p.  435,  pi.  16. 

Proetus  bowningensis,  Cyphaspis  bownin- 
gensis,  Bronteus  longispinifer. 

On  a new  Trilobite  from  Bcwning. 

In  Proc.  Linnean  Soc.  Hew  South  Wales,  2d 
series,  vol.  3,  1888,  p.  397,  pi.  16  of  vol.  2. 

Acidaspis  longispinis. 

Mitchell  (Samuel  L.)  An  account  of  the 
impressions  of  a fish  in  the  rocks  of 
Oneida  County,  New  York. 

In  Am.  Monthly  Mag.,  vol.  3,  1818,  p.  291. 

The  author  states  that  the  Hew  York  fossil, 
from  the  town  of  Westmoreland,  “is  separated 
into  plates,  like  those  of  an  insect  or  crusta- 
ceous  animal,  reaching  from  side  to  side  quite 
across  the  back.  Eleven  entire  plates  and  part 
of  the  twelfth  can  be  counted.  They  are  not  so 
broad  near  the  head  and  thorax  as  they  are  on 
approaching  the  tail ; for  between  the  pectoral 
fins  they  fall  short  of  a quarter  of  an  inch, 
while  on  approaching  the  caudal  fin  they  grad- 
ually enlarge  until  they  exceed  that  measure.” 

Eurypterus  remipes  De  Kay. 

Modeer  (A.)  Anmerkungen  fiber  einige 
nerikische  Versteiner ungen.  (*) 

In  Berlin.  Gesell.  naturf.  Freunde,  vol.  6, 
1785,  p.  247,  pi.  2,  figs.  1-8-12. 

(Agnostus  pisiformis),  pi.  2,  figs.  1,  2 ; (Olenus 
gibbosus),  pi. 2,  figs.  3-5;  (Olenus  scaraboeoides), 
pl.  2,  fig.  7. 

Moller  (Valerian  von).  Ueber  die  Trilo- 
biteu  der  Steinkohlenformation  des 
Ural,  nebst  einer  Uebersicht  und  eini- 
gen  Ergiinzungen  der  bisherigen  Beob- 
achtuugen  fiber  Kohlen-Trilobiten  im 
Allgemeinen.  Moscou,  1867.  1 pl. 

In  Bull.  Soc.  Imp.  des  Haturalistes  Moscou, 
Ho.  1, 1867. 

Qrijjlthides,  Phillipsia , Brachymetopus. 

Morris  ( J. ) Catalogue  of  British  fossils. 
London,  1843.  2d  ed.,  London,  1854. 


54 


A BIBLIOGRAPHY  OF  PALEOZOIC  CRUSTACEA. 


[bull..  63. 


Mortimer  (C.)  The  description  and  fig- 
ures of  a small,  flat,  spheroidal  stone 
having  lines  formed  on  it. 

In  Philos.  Trans.  Royal  Soc.  London,  voL 
46,  1760,  p.  602,  pis.  1,  2. 

( Calymene  blumenbachi.) 

Miiller  (O.  F.)  Entomostraca  sen  insecta 
testacea  quse  in  aquis  Daniae  et  Nor- 
wegiae  reperit,  etc.  Lipsiae  et  Hafniae, 
1785.  21  pis. 

Cythere  n.  g. 

The  generic  term  Cytherina  was  substituted 
by  Lamarck  for  Muller’s  Cythere,  and  has  been 
used  by  many  authors.  Prof.  J.  D.  Dana  uses 
the  term  Cytherina  to  represent  a subgenus. 

Munster  (G.  G.)  Ueber  einige  fossile 
Arten  Cypris  und  Cythere. 

In  Jahrbuch  fur  Mineral.,  1830,  p.  60. 

Cythere  hissingeri. 

and  Meyer  (H.  von).  See  Meyer 

and  Miinster. 

Murchison  (R.  I.)  The  Silurian  system, 
founded  on  geological  researches  in 
the  counties  of  Salop,  Hereford,  Rad- 
nor, q^fcc.  [London,  2 vols.,  1839,  40 
pis.,  and  3 larg c maps  in  folio.] 

Calymene,  Homalonotus,  Asaphus,  Ogygia, 
Illcenus,  JBumastus  n.  g.,  Acidaspis  n.  g.,  Trinu- 
cleus n.  g.,  Agnostus. 

Metamorphosis  of  certain  Trilobites 

as  recently  discovered  by  M.  Barrande. 

In  Rept.  19th  Meeting  Brit.  Assoc.  Adv. 
Sci.,  1849,  Trans.  Sec.,  p.  58. 

On  the  Silurian  rocks  of  the  south 

ot  Scotland,  with  a list  and  descrip- 
tion of  the  Silurian  fossils  of  Ayrshire, 
by  J.  W.  Salter. 

In  Quart.  Jour.  Geol.  Soc.  London,  vol.  7, 
1851,  p.  137,  pis.  8-10. 

Cheirurus  gelasinosus  Port.,  Asaphus  sp.  1, 
Calymene  blumenbachi  Brong.,  Phacops  stokesii 
Milne -Edwards,  Illcenus  bowmani? , Lichas 
laxatus  McCoy,  Encrinurus  punctatus  Briin. 

Siluria.  A history  of  the  oldest 

rocks  in  the  British  Isles  and  other 
countries.  [London,  1854,  geol.  map, 
37  pis.  3d  ed.,  London,  1859,  geol. 
map,  41  pis.  4th  ed.,  London,  1867, 
geol.  map,  42  pis.] 

The  figures  are  all  transferred  from  the 
original  plates  in  the  “Silurian  system.”  In 
every  case  where  the  old  name  has  been 
changed,  in  accordance  with  more  recent  no- 
menclature, the  name  used  in  the  original 
work  is  inserted  in  brackets. 

, Verneuil  (E.  de)  and  Keyserling 

(Alex.  von).  Geology  and  palaeontol- 
ogy of  Russia  and  the  Ural  Mountains. 


Murchison  (R.  I.)  and  Verneuil  (E.  de) — 
Continued. 

[London,  1845,  2 vols.,  50  pis.  Palae- 
ontology, vol.  2;  Crustacea,  p.  376, 
pi.  27.] 

Asaphus  expansas  Dalm.,  Phillipsia  eich- 
waldi  Fischer,  P.  ouradica  n.  s.,  Calymene- 
odeni  Eichw.,  O.  fischeri  Eichw. 

Nathorst  (A.  G. ) Om  lager-foljden  inom 
i Cambriska  formationen  vid  Andrarum 
I i Skane. 

In  Ofversigt  kongl.  Svenska  Vet.-Akad.  For- 
handl.,  1869,  No.  1,  p.  61. 

Om  de  Kambriska  och  Siluriska  la- 

gren  vid  Kiviksesperid  i Skane  jeuite 
anmarkningar  om  primordial  faunans 
lager  vid  Andrarum. 

In  Geol.  Foreningens  Stockholm  Forhandl., 
No.  37,  vol.  3, 1876. 

Om  det  inbordes  forhallandet  af  la- 

gren  med  Paradoxides  olandicud  och  P.  _ 
tessini  pa  Oland. 

In  Geol.  Foreningens  Stockholm  Forhandl., 
No.  69,  vol.  5, 1881. 

Om  det  iubordes  aldersforhallandet 

mellan  zonerna  med  Olenellus  kjerulfi 
och  Paradoxides  olandicus. 

In  Geol.  Foreningens  Stockholm  Forhandl., 
No.  71,  vol.  6, 1882. 

The  position  of  the  Olenellus  beds. 

In  Am.  Geol.,  vol.  2, 1888,  p.  356. 

Newberry  (J.  S.)  China,  by  Ferdinand 
F.  von  Richthofen.  Vol.  4.  Berlin,  I 
1883.  * 

In  Am.  Jour.  Sci.,  3d  series,  vol.  26, 1883,  p. 
152. 

This  is  a notice  of  the  palaeontological  vol- 
ume. 

Nicholson  (H.  A.)  A manual  of  palaeon-  I 
tology  for  the  use  of  students,  with  a : 
general  introduction  on  the  principles  9 
of  palseon tology,  in  two  volumes.  Vol.  | 
1.  Edinburgh  and  London,  1879.  Cru-  I 
stacea,  Chapter  xvm. 

Harpes,  Remopleurides,  Paradoxides,  Anopo - | 
lenus,  Dicellocephalus,  Hydrocephalus,  Olenua,  I 
Parabolina,  Triarthrus,  Bohemilla,  Conocepha-' I 
lites,  Angelina,  Ellipsocephalus,  Sao,  Proetua,  j 
Arethusina,  Phillipsia,  GriJJithides,  Bathymeto-  I 
pus,  Phacops,  Dalmanites,  Calymene,  Homalo-  I 
notus,  Lichas,  Trinucleus,  Ampyx,  Dionide,  I 
JEglina,  Asaphus,  Ogygia,  Barrandia,  Niobe,  I 
N ileus,  Stygina,  Illcenus,  Acidaspis , Cheirurus,  I 
Sphcerexochus,  Areia,  Placoparia,  Cromus,  En-  j 
crinurus,  Cybcle,  Dindymcne,  Bronteus,  Agnoa-  I 
tus,  Microdiscus,  Protichnites,  Ai’istozoe,  Beyri-  I 
chia,  Leperditia,  Primitia,  Entomis,  Cythere , I 
Eurypterus,  Pterygotus,  Isochilina,  Cypris,  I 
Candona,  Orozoe,  Callizoe,  Kirkbya,  Moorea,  R 
Cryprulina,  Cytherella,  Cytherellina,  AZchmina,  H 

H 


VOGDK6.J 


LIST  OF  AUTHORS. 


55 


Nicholson  (H.  A.)  Continued. 

Bairdia,  Hymenocaris,  Caryocaris,  Peltocaris, 
Pisdnocaris,  Aptychopis,  Pterocaris , Gryptoca- 
ris,  Ceratiocaris,  Pithyrocaris,  Aspidocaris,  Es- 
theria,  Psilocephalus , Hemiaspis,  Exapinurus , 
Pseudoniscus,  Stylonurus , Neolimulus,  Prestwi- 
chia , Belinurus. 

and  Etheridge,  jr.  (R.)  A mono- 
graph of  the  Silurian  fossils  of  the  Gi- 
van  District,  in  Ayeshire,  etc.  Vol.  1, 
1878-’80,  24  pis. 

Fasciculus  I.  Rhizopoda,  Actinozoa,  and 
Trilobites  (1878). 

Phacops,  Calymene,  Lichas , Pindymene, 
Asaphus,  Ogygia , Acidaspis,  Gheirurus,  Sphce- 
rexochus,  Encrinurus , Cybele , Zethus,  Atracto- 

pyge- 

Fasciculus  II.  Trilobita,  Phyllopoda,  Cir- 
ripedia,  and  Oslracoda  (1879). 

Bemopleu  rides  ( Gaphyra ),  Proetus,  Cyphas- 
pis,  Phacops , Calymene,  Lichas,  Trinucleus , 
Ampyx,  Salteria,  Asaphus,  Illoenus,  Gheirurus, 
Acidaspis,  Encrinurus,  Cybele,  Bronteus , Ag- 
nostus,  Bronteopsis,  Lonchodomus,  Raphiopho- 
nes,  Solenocaris,  Pinnocaris  Peltocaris,  Piety  o- 
caris,  Turrilepas,  Beyrichia,  Primitia,  Gythere, 
Entomis. 

Fasciculus  III.  The  Annelida  and  Echino- 
dermata,  with  supplements  on  the  Protozoa, 
Coelenterata,  and  Crustacea  (1880). 

Trinucleus,  Pionide,  Cyclopyge,  Staurocepha- 
lus,  Agnostus , Turrilepas. 

Nieszkowski  (J.)  Der  Eurypterus  remi- 
pes  aus  den  ober-silurischen  Schichten 
der  Insel  Oesel. 

In  ArchivNaturk.  Liv-,  Ehst-  u.  Kurl.,  vol.  2, 

1858,  p.  299,  2 pis. 

VersoCh  einer  Monographie  der  in 

den  silurischen  Schichten  der  Ostsee- 
provinzen  vorkommenden  Trilobiten. 

In  ArcbivNaturk.  Liv-,  Ehst-  u.  Kurl.,  vol.  1, 
1857,  p.  517,  3 pis. 

Proetus,  Cyphaspis,  Phacops,  Calymene,  Li- 
chas, Asaphus,  Illoenus,  Gheirurus,  Sphcerexo- 
chus,  Amphion,  Encrinurus,  Zethus,  Bronteus, 

Platymetopus. 

Zusatze  zur  Monographie  der  Trilo- 
biten der  Ostseeprovinzen,  nebst  der 
Beschreibung  einiger  neuen  ober- silu- 
rischen Crustaceen. 

In  ArchivKaturk.  Liv-,  Ebst  u.  Kurl.,  vol.  1, 

1859,  p.  345,  2 pis. 

Cyphaspis,  Lichas,  Asaphus,  Gheirurus,  Sphce - 
rexochus,  Encrinurus,  Bronteus,  Bunodes,  Exa~ 
pinurus  n.  g.,  Pseudoniscus  n.  g. 

Novak  (Ottomar).  Studien  an  Hyposto- 
men  bdhmischer  Trilobiten.  No.  1. 

In  Sitzungsberichte  k.  bohm.Gesell.  Wiss., 

Jahrg.  1879,  p.  475. 


Novak  (Ottomar) — Continued. 

Harpes,  Paraaoxides,  Oonocephalites,  Proetus, 
Palmanites,  Trinucleus,  Ampyx,  Acidaspis, 
Gheirurus,  Placoparia,  Bronteus,  Garmon, 
Harpina  n.  g.,  Galymene,  Illoenus,  Phacops. 

Studien  an  Hypostomen  bohmischer 

Trilobiten.  No.  2. 

In  Sitzungsberichte  k.  bohm.  Gesell.  Wiss., 
Jahrg.  1884,  1 pi. 

ILarpes,  Harpina,  Asaphus,  Ogygia , Niobe. 

Zur  Kenntniss  der  bohmischen  Trilo- 
biten. 

In  Beitrage  zur  Palaeontolographie  von 
Oesterrich,  Wien,  1884,  5 pis. 

Harpes,  Remopleurides , Phillipsia,  Dalmani- 
tes,  Galymene,  Homalonotus,  JEglina,  Trinu- 
cleus, Ampyx,  Pionide,  Asaphus,  Barrandia, 
Ptychocheilus,  Illoenus,  Acidaspis,  Gheirurus , 
Placoparia,  Cromus , Bronteus,  Agnostus. 

Studien  an  Hypostomen  bohmischer 

Trilobiten.  No.  3. 

In  Sitzungsberichte  k.  bohm.  Gesell.  Wiss., 
Jahrg.  1885,  p.  581,  1 pi. 

Phillipsia,  Phillip sinella  n.  g. 

Remarques  sur  le  genre  Aristozoe 

Barrande. 

In  Sitzungsberichte  k.  bohm.Gesell.  Wiss., 
Jahrg.  1885,  p.  239, 1 pi. 

Aristozoe,  Oallizoe,  Ceratiocaris,  Orozoe. 

Nouveau  Crustac6  phyllocaride  de 

F6tage  F-f2  en  Boheme. 

In  Sitzungsberichte  k.  bohm.  Gesell.  Wiss., 
Jahrg.  1885,  p.  343, 1 pi. 

Ptychocaris  n.  g. 

Studien  an  Hypostomen  bohmischer 

Trilobiten.  No.  4. 

In  Sitzungsberichte  k.  bohm.  Gesell.  Wiss., 
Jahrg.  1886,  p.  429,  plate. 

Encrinurus,  Cromus. 

Zur  Kenntniss  der  Fauna  der  Rtage 

F-fi  in  der  paheozoischen  Schichten- 
gruppe  Bohmens. 

In  Sitzungsberichte  k.  bohm.  Gesell.  Wiss., 
Jahrg.  1886,  p.  660,  2 pis. 

Aristozoe. 

Note  sur  Phasganocaris,  nouvoau 

Phyllocaride  de  P6tage  F-f2  en  Bo- 
h§rae. 

In  Sitzungsberichte  k.  bohm.  Gesell.  Wiss., 
Jabrg.  1886,  p.  498,  1 pi. 

Phasganocaris  n.  g. 

Oehlert  (D.)  Sur  lea  fossiles  d6voniens 
du  ddpartement  de  la  Mayeune. 

In  Bull.  Soc.  G6ol.  France,  3d  series,  vol.  5, 
1877,  p.  578,  pi.  9. 

Gryphceus  michelini,  C.  jonesi.  G.  munieri, 
Homalonotus  gervillei,  Leperditia  britannica, 
Primitia  fischeri. 


56 


A BIBLIOGRAPHY  OF  PALEOZOIC  CRUSTACEA, 


[BUIjL.  63. 


Oehlert  (D.)  Sur  le  D6vonien  du  d6- 
partement  de  la  Sartlie. 

In  Bull.  Soc.  G6ol.  France,  3d  series,  vol.  7, 
1879,  p.  697,  pi.  13. 

Proetus  guerangeri , Bronteus  verneuili. 

Description  de  Goldins  gerville  Bar- 

rande. 

In  Bull.  Soc.  d’E tudes  Sei.,  Angers,  1885, 1 pi. 

Etudes  sur  quelques  Trilobites  du 

groupe  des  Proetidse. 

In  Bull.  Soc.  d’Etudes  Sci.,  Angers,  1885, 2 pis. 

The  author  divides  the  Proetidae  into  two 
divisions  on  the  form  of  the  glabella. 

Sec.  A.  Glabella  conic,  genera  Proetus,  Phce- 
ton,  Dechenella,  and  Brachymetopus. 

Sec.  B.  Glabella  pyriform,  genera  Phillip - 
sella,  Phillip sia,  and  Griffithides. 

Harpes,  Gonocephalites,  Gyphaspis,  Arethu- 
sina,  Galymene,  Asaphus,  Ogygia,  Bronteus. 

Etudes  sur  quelques  fossiles  d6vo- 

niens  de  l’ouest  de  la  France. 

In  Bibliotheque  de  l’Eeole  des  Hautes 
Etudes,  Sec.  Sci.  Nat.,  vol.  33, 1887,  5 pis. 

Proetus  oehlerti  Bayle,  Phacops  portieri 
Bayle. 

Oldham  (4T.)  On  Griffithides  glohiceps. 

In  Jour.  Geol.  Soc.  Dublin,  vol.  3,  pt.  3, 1846, 
p.  188,  pi.  2. 

Redrawn,  pi.  6,  fig.  la,  b, Woodward’s  “Mono, 
graph  British  Carboniferous  Trilobites,”  Lon- 
don, 1883. 

Ordway  (Albert).  On  the  supposed 
identity  of  Paradoxides  harlani  Green 
with  P.  spino8us  Boeck. 

In  Proc.  Boston  Soc.  Nat.  Hist.,  vol.  8,  1861, 
p.  1,  2 figs. 

The  organization  of  the  Trilobites. 

In  Geol.  Nat.  Hist.  Repertory,  vol.  1,  1865,  p. 

12. 

Owen  (D.  D.)  Report  of  a geological  ex- 
ploration of  part  of  Iowa,  Wisconsin, 
and  Illinois,  made  under  instructions 
from  the  Secretary  of  the  Treasury  of 
the  United  States,  in  the  autumn  of  the 
year  1839.  Washington,  1840. 

In  26th  Cong.,  H.  of  Rep.,  Doc.  239,  2d  ed., 
1844;  28th  Cong.,  Sen.  Doc.  407,  18  pis.  of 
fossils. 

PI.  12,  fig.  3,  Galymene  bufo;  pi.  16,  fig.  1, 
llloenus  trentonensis?  (referred  by  Dr.  D.  D. 
Owen,  in  1852,  to  llloenus  ovalis);  pi.  17,  fig.  9, 
Thaleops?;  pi.  18,  fig.  2,  Asaphus,-  pi.  18,  fig.  10 
(Asaphus  platycephalus)  -,  pi.  18,  fig.  2,  Asaphus. 

Report  of  a geological  reconuois- 

sance  of  the  Chippewa  Land  District  of 
Wisconsin  and  incidentally  of  a portion 
of  the  Kickapoo  country,  and  a part  of 
Iowa  and  of  the  Minnesota  territory, 
etc.  Washington,  1848. 


Owen  (D.  D.) — Continued. 

This  report  contains  figures  of  the  following 
fossils,  which  were  afterwar  s described  by 
Dr.  D.  D.  Owen  under  the  names  of  Dikelo- 
cephalus  minnesotensis,  pi.  7 .figs.  2,  3 ; Loncho- 
cephalus  hamulus,  pi.  7,  fig.  5;  Dikelo  cephalus 
iowensis,  pi.  7,  fig.  1. 

Report  of  a geological  survey  of  Wis- 
consin, Iowa,  and  Minnesota,  and,  inci- 
dentally, a portion  of  Nebraska  Terri- 
tory. Philadelphia,  1852,  638  pp.,  27 
pis.,  16  sections  and  maps. 

Dikelocephalus  n.  g.,  Loncho  cephalus  n.  g.t 
Grepicephalus  n.  g.,  Menocephalus  n.  g.,  Asa- 
phus ( Isotelus)  iowensis. 

Owen  (Richard).  Description  of  the  im- 
pressions and  foot-prints  of  the  Protich- 
nites  from  the  Potsdam  sandstone  of 
Canada. 

In  Quart.  Jour.  Geol.  Soc.  London,  voL  8, 1852, 
p.  214,  pis.  9-14a. 

Palaeontology,  or  a systematic  sum- 
mary of  extinct  animals  and  their 
geological  relation.  Edinburgh,  1861. 

Class  3.  Crustacea,  pp.  45-51. 

Facht  (R.)  Geognostische  Untersuchun- 
gen  zwischen  Orel  Woronasch  und  Sim- 
birsk im  Jahre  1853. 

In  Beitrage  zur  Kenntniss  des  russischen 
Reiches  und  der  angranzenden  Lander  Asiens, 
St.  Petersburg,  1858. 

Packard,  jr.  (A.  S.)  On  the  embryology 
of  Limulus  polyphemus. 

In  Proc.  Am.  Assoc.  Adv.  Sci.,  1870,  19th 
meeting,  p.  247. 

Notes  on  the  larva  of  Trilobites,  etc. 

The  structure  of  the  eye  of  Trilo- 
bites. 

In  Am.  Naturalist,  vol.  14,  1880,  p.  503. 

A monograph  of  the  Phyllopod  Crus- 
tacea of  North  America,  with  remarks 
on  the  order  Phyllocarida.  Pis.  1-38. 

In  Twelfth  Rept.  TJ.  S.  Geol.  Survey  Teiri- 
tories  (Hayden),  Washington,  1883,  pt.  1,  p.  295. 

Hymenocaris,  Peltocaris,  Oeratiocaris,  Echi - 
nocaris,  Discinocaris,  Spathiocaris,  Lisgocaris , 
Aptychopsis,  Dictyocaris,  Dithyrocaris,  Ra- 
chura,  Argus,  Estheria,  Leaia. 

Types  of  Carbouiferous  X iphosura 

new  to  North  America. 

In  Am.  Naturalist,  vol.  19,  1885,  p.  291.“ 

Belinurus,  Euproops,  Oyclus,  Dipeltis  n.  g. 

The  Syncarida,  a group  of  Carbonif- 
erous Crustacea. 

In  Am.  Naturalist,  vol.  19,  1885,  p.  700. 

Acanthotelson. 


VOGUES.] 


LIST  OF  AUTHORS. 


57 


Packard,  jr,  (A.  S.)— Continued. 

On  the  Gampsonychidce , an  unde- 
scribed family  of  fossil  Schizopod  Crus- 
tacea. 

In  Am.  Naturalist,  vol.  19, 1885,  p.  790 ; Mem. 
Nat.  Acad.  Sci.,  vol.  3,  1886,  p.  129,  pi.  3. 

Palceocaris,  Qampsonyx. 

On  the  Anthracoridce,  a family  of 

Carboniferous  Alacrurous  decapod  Crus-  j 
tacea  allied  to  the  Eryovidw. 

In  Am.  Naturalist,  vol.  19,  1885,  p.  880 ; Mem. 
Nat.  Acad.  Sci , vol.  3,  1886,  p.  135,  pi.  4. 

Anthrapalcemon. 

Discovery  of  the  thoracic  feet  in  a 

Carboniferous  Phyllocaridan. 

In  Am.  Philos.  Soc.,  vol.  23, 1886,  p.  380,  plate. 

Oryptozoe  problematicus. 

On  the  class  Podostomata,  a group 

embracing  the  Merostomata  and  Trilo- 
bites. 

In  Am.  Naturalist,  vol.  20,  1886,  p.  1060. 

Merostomata : Xiphosura,  Synziphosura,  Eu- 
rypteridce. 

On  the  Syncarida,  a hitherto  unde- 
scribed synthetic  group  of  extinct  Ma- 
lacostracous  Crustacea. 

In  Mem.  Nat.  Acad.  Sci.,  vol.  3,  pt.  2,  1886,  p. 
123,  pis.  1, 2. 

Acanthotelson. 

On  the  Carboniferous  Xiphosurous 

fauna  of  North  America. 

In  Mem.  Nat.  Acad.  Sci.,  vol.  3,  pt.2, 1886,  p. 
143, 8 figs.,  3 pis. 

Cyclus,  Dipeltis,  Prestwichia,  Belinurus, 
Palceocaris,  Anthrapalcemon,  Protolimulus  n. 
g.,  Bunodes,  Pseudoniscus,  Exapinurus,  Hemi- 
aspis,  Neolimulus. 

Page  (David).  On  the  Pterygotus  and 
Pterygotus  beds  of  Great  Britain. 

In  Kept.  25th  Meeting  Brit.  Assoc.  Adv.  Sci., 
1855,  Trans.  Sec.,  p.  89. 

The  genus  Stylonurus  was  proposed  by  Mr. 
David  Page  in  his  paper  read  before  the  Asso- 
ciation, and  the  name  published  in  his  “Ad- 
vance text-book  of  geology,”  1856. 

Further  contributions  to  the  palae- 
ontology of  the  Tilestones  or  Silurio- 
Devonian  strata  of  Scotland. 

In  Kept.  28th  Meeting  Brit.  Assoc.  Adv.  Sci., 
Trans.  Sec.,  p.  104. 

Beyrichia,  Oeratiocaris,  Himantopterus,  Sty- 
lonurus tpinipes,  S.  clavipes,  Kampecaris,  Eu- 

ryp  torus. 

Advance  text-book  of  geology.  Lon- 
don, 1856. 

Slimonia  n.  g.,  Stylonurus  n.  g.,  Kampecaris, 
Himantopterus,  Pterygotus,  Parka. 


Page  (David) — Continued. 

In  the  second  edition,  1859,  Mr.  David  Page 
gives  restorations  of  Pterygotus  anglicus,  Hi- 
mantopterus acuminatus,  Stylonurus  powriei, 
S.  spinipes,  Eurypterus  clavipes,  E.  scouleri,  and 
Limulus  rotundatus. 

Note  on  the  genus  Stylonurus  from 

the  Old  Red  Sandstone  of  Forfarshire. 

In  Proc.  Royal  Phys.  Soc.  Edinburgh,  session 
1864-’65,  p.  230. 

Pander  (C.  H.)  Beitriige  zur  Geogno- 
sie  des  russischen  Reiches.  St.  Peters- 
burgh,  1830 ; Leipzig,  1839,  31  pis. 

Calymene,  Asaphus,  Illcenus,  Nileus,  Am- 
phion  n.  g. , Zethus  n.  g. 

Parkinson  (James).  Organic  remains 
of  a former  world,  an  examination  of 
the  mineralized  remains  of  the  vege- 
table and  animal  antediluvian  world 
generally  termed  extraneous  fossils. 
London,  1808,  3 vols.  Crustacea,  vol, 
3,  letter  16*,  pi.  17. 

Calymene,  Ogygia,  Encrinurus,  Phacops, 
Belinurus. 

Payton.  ( — ).  Trilobites  found  in  the 
Transition  limestone  at  Dudley,  from 
the  collection  of  Mr.  Payton,  at  Dudley. 
London,  1827,  2 pp.,  2 pis. 

Calymene  blumenbachii  and  Asaphus  cau- 
datus. 

Peach  (B.  N.)  On  some  new  Crustaceans 
from  the  Lower  Carboniferous  rocks  of 
Eskdale  and  Liddesdale. 

In  Trans.  Royal  Soc.  Edinburgh,  vol.  30,  pt. 
1,  1880,  p.  73,  4 pis. 

Oeratiocaris,  Anthrapalcemon,  Palceocran- 
gon,  Palceocaris,  Uronetes. 

Further  researches  among  the  Crus- 
tacea and  Arachnida  of  the  Carbonif- 
erous rocks  of  the  Scottish  border. 

In  Trans.  Royal  Soc.  Edinburgh,  vol.  30,  pt. 
2, 1880,  p.  511,  2 pis. 

Prestwichia,  Cyclus,  Eurypterus,  Olyptoscor- 
pius  n.  g.,  Acanthocaris  n.  g.,  Anthrapalcemon, 
Palceocrangon,  Palceocaris,  Pseudo  - Qalathea 
n.  g. 

On  the  occurrence  of  Pterygotus  and 

a Limuloid  in  the  Caithness  Flagstones, 
and  on  the  nature  and  mode  of  forma- 
tion of  “Adam’s  plate.” 

In  Proc.  Royal  Phys.  Soc.  Edinburgh,  1883, 
p.  343,  plate. 

Pterygotus  dicki. 

Phillips  (John).  On  the  occurrence  of 
some  minute  fossil  Crustaceans  in  Pa- 
laeozoic rocks. 

In  Rept.  11th  Meeting  Brit.  Assoc.  Adv.  Sci., 
1841,  Trans.  Sec.,  p.  64. 


58  A BIBLIOGRAPHY  OF  PALEOZOIC  CRUSTACEA.  [bull.  63. 


Phillips  (John)— Continued. 

Illustrations  of  the  geology  of  York- 
shire. Pt.  2.  The  mountain  limestone 
district.  London,  1836,  p.  239. 

Asaphus  ( Phillipsia ). 

Figures  and  descriptions  of  the 

Palaeozoic  fossils  of  Cornwall,  Devon, 
and  West  Somerset,  observed  in  the 
course  of  the  Ordnance  Geological  Sur- 
vey of  that  district.  London,  1841,  60 
pis.  Crustacea,  p.  127. 

Harpes,  Calymene  ( Ceraurus , Phacops), 
Homalonotus,  Asaphus,  Bronteus. 

The  Malvern  Hill  compared  with  the 

Palaeozoic  district  of  Abberley,  Wool- 
hope,  May  Hill,  Tortworth,  and  Usk. 

In  Mem.  Geol.  Survey  Gt.  Brit.,vol.  2,  pt.  1, 
London,  1848.  Palaeontological  appendix  to 
Prof.  John  Phillips’s  memoir  on  the  “ Malvern 
Hills  compared  with  the  Palaeozoic  district  of 
Abberley,”  etc.,  by  John  Phillips  and  J.  W. 
Salter.  Ibid.,  pp.  331-386,  30  pis. 

For  list  of  genera,  see  Salter  (J.  W.)  and 
Phillips  ( J ohn). 

Manual  of  geology.  Pt.  2.  Ed.  by 

Rob.  Etheridge.  1885,  pis.  1-12. 

Paradoxides,  Olenus , Asaphus,  Ogygia,  Caly- 
mene, Trinucleus,  Agnostus,  Illsenus,  Lichas,  | 
Beyrichia,  Stygina,  Phacops,  Cybele , Cheirurus, 
Bemopleur  des,  Harpes,  Ampyx,  Acidaspis,  Cy- 
phoniscus,  JEglina,  Sphcerexochus,  Encrinurus, 
Cyphaspis,  Proetus,  Pterygotus,  Bronteus , 
Homalonotus,  Phillipsia. 

Pictet  (F.-J.)  TraitA  de  pal^ontologie, 
ou  histoire  naturelle  des  animaux  fos- 
siles  consider  As  dans  leurs  rapports 
zoologique  et  g^ologique.  4 vols  and 
atlas.  Paris,  1853-’57.  Crustacea,  vol. 
2,  1854,  p.  413. 

The  author  arranges  the  families  and  genera 
as  follows:  Harpidae:  Harpes.  Paradoxidae: 
Bemopleurides,  Paradoxides,  Hydrocephalus, 
Sao,  Arionellus,  Ellipsocephalus,  Olenus,  Pel- 
tura,  Triarthrus,  Conocephalites.  Caiymeuidae, 
1st  section,  Proetidae  : Proetus,  Phillipsia,  Cy- 
phaspis, Arethusina,  Harpes ; 2.1  section,  Pha- 
copidaB : Phacops,  Dalmania ; 3d  section,  Caly- 
menid&e:  Calymene,  Homalonotus.  Lichasidae. 
Lichas.  Trinucleidae:  Trinucleus,  Ampyx,  Dio- 
nide.  Asaphidae : Asaphus,  Symphysurus, 
Ogygia.  iEglinidae:  JEglina.  Illaenidae:  lllce- 
nus,  Nileus.  Odontopleuridae : Acidaspis,  Chei- 
rurus, Placoparia,  Sphcerexochus,  Staurocepha- 
lus,  Deiphon,  Zethus,  Dindymene.  Amphioni- 
dae : Amphion,  Cromus,  Encrinurus.  Bronti- 
dae  : Bronteus.  Agnostidae : Agnostus.  Phyllo- 
podae : Apusiens,  Dithyrocaris,  Apus,  Estheria, 
Copepodae : Eurypterus.  Cypi’oidaB : Cythere, 
Bairdia,  Beyrichia,  Leperditia,  Cypris.  Cypri- 
dinae : Cyprella,  Oypridella.  Xiphosurae : Li- 
mulus,  Belinurus,  Pterygotus.  Amphipodae : 
Qampsonyx. 


Pitt.  See  Grote  and  Pitt. 

Plant  (John).  On  the  discovery  of  Para- 
doxides davidis  at  Tyddyngwladis,  near 
Dolgelly,  North  Wales. 

In  Trans.  Manchester  Geol.  Soc.,  vol.  5, 1886, 
p.  76. 

Pohlman  (Julius).  On  certain  fossils  of 
the  Waterlime  group  near  Buffalo. 

In  Bull.  Buffalo  Soc.  Nat.  Sei.,  vol.  4, 1881,  p. 
17, 7 figs. 

Pterygotus  buffaloensis,  Ceratiocaris  grandis. 

Additional  notes  on  the  fauna  of  the 

Waterlime  group. 

In  Bull.  Buffalo  Soc.  Nat.  Sci.,  vol.  4,  1882,  p. 
41,  2 pis. 

Eurypterus  giganteus,  Pterygotus  globicauda- 
tus,  P.  acuticaudatus,  P.  quadraticaudatus,  P. 
macrophthalmus?,  P.  buffaloensis. 

Fossils  from  the  Waterlime  gtoup 

near  Buffalo,  N.  Y. 

In  Bull.  Buffalo  Soc.  Nat.  Sci.,  vol.  5,  1886,  p. 
17,  pi.  3. 

Pterygotus  buffaloensis,  P.  bilobus,  Ceratioca- 
ris acuminatus,  Eusarcus,  E.  grandis,  Eurypte- 
rus scorpionis  (the  term  Eurypterus  scorpioe- 
des  was  used  by  Henry  Woodward  for  a species 
of  this  genus  in  1868.  See  Eurypterus  pohl- 
mani). 

Portlock  (J.  E.)  Report  on  the  geology 
of  the  county  of  Londonderry,  and  of 
parts  of  Tyrone  and  Fermanagh.  Dub- 
lin, 1843,  28  pis.,  also  maps  and  sections. 

Harpes,  Bemopleurides  n.  g.,  Proetus,  Phillip- 
sia n.  g.,  Griffithides  n.  g.,  Phacops,  Calymene, 
ges,  Trinucleus,  Ampyx,  Nuttainia,  Asaphus, 
Isotelus,  Ogygia,  Ceraurus,  Amphion,  Zethus, 
Brontes,  lllcenus,  Dithyocaris  (Seoul er)  Port- 
lock,  Limulus. 

Postlethwaite  (J.)  and  Goodchild  (J. 
G.)  On  some  Trilobites  from  the  Skid- 
daw  slates. 

In  Proc.  Geologist  Assoc.,  vol.  9,  No.  7,  1886, 
p.  455,  pis.  6-9. 

In  this  contribution  the  initials  of  each  au- 
thor designate  the  paragraphs  written  by  him. 

The  following  list  is  given  of  the  Trilobite 
fauna  of  the  Skiddaw  slates : 

Phacops nicholsoni  Salter,  Cybele  ovata  Ether- 
idge, Calymene  brevicapitata  ? , Bemopleurides 
sp.  ? , Olenus  sp.  ? , Trinucleus  gibbsii  ?,  Ogygia 
selwyni,  Ogygia  sp.  ?,  Barrandia  falcata  P.  & 
G.,  Niobe  doveri  Eth.,  Eurymetopus  cambrianus 
n.  g.  and  n.  sp.  P.  & G.,  E.harrisonii  P.  A G., 
JEglina?  rediviva  Barr.,  A.  binodosa,  A.  obtu- 
sicauda  Hicks,  A.?  caliginosa,  Agnostus .morei 
Salter. 

Prestwich  (S.)  On  the  geology  of  Coal- 
brook  Dale. 

In  Trans.  Geol.  Soc.  London,  vol.  5,  1840,  p. 
413,  map,  2 sections,  4 pis. 

Belinurus. 


V0GDES.1 


LIST  OF  AUTHORS. 


59 


Quenstedt  (F.  A.)  Beitrage  zur  Kennt- 
niss  der  Trilobiten.  Riicksicht  auf  ihre 
bestimmte  Gliederzahl. 

In  Arcliiv  fiir  Naturgesch.  (Wiegmann), 
vol.  1,  Berlin,  1837,  p.  337. 

In  this  work  Prof.  F.  A.  Quenstedt  divides 
the  Trilobites  into  two  groups:  1.  Trilobites 
with  faceted  eyes;  2.  Trilobites  with  non- 
faceted  eyes.  The  genera  are  classified  accord- 
ing to  the  number  of  segments  in  the  thorax. 

Rafinesque  (C.  S.)  On  the  genera  of  fos- 
sil Trilobites  or  Glomerites  of  North 
America. 

In  Atlantic  Jour,  and  Friend  to  Knowledge, 
vol.  1,  1832,  p.  71. 

Ramsay  (A.  C.)  The  geology  of  North 
Wales,  with  an  appendix  on  the  fossils; 
with  plates  by  J.  W.  Salter. 

In  Mem.  Geol.  Survey  Gt.  Brit.,  vol.  3,  1866. 

Di/celocephalus,  Olenus,  Parabolina,  Cono- 
coryphe,  Angelina , Homalonotus,  Lichas,  Trinu- 
cleus, Dionide,  Ampyx,  Asaphus,  Kiobe,  JEglina, 
Cheirurus , Encrinurus , lllcenus,  Agnostus,  Psi- 
locephalus,  Beyrichia,  Hymenocaris. 

Rathbun  (Richard).  See  Hartt  (C.  F.) 
and  Rathbun  (Richard). 

Ratte  (F.)  Note  on  some  Trilobites  new 
to  Australia. 

In  Proc.  Linn.  Soc.  New  South  Wales,  2d 
series,  vol.  1,  1886,  p.  1067,  3 pis. 

Lichas,  Proetus,  Acidaspis. 

Note  on  some  Trilobites  new  to  Aus- 
tralia. 

In  Proc.  Linn.  Soc.  New  South  Wales,  2d 
series,  vol.  2,  1887,  p.  95,  2 pis. 

Lichas,  Acidaspis,  Staurocephalus. 

Razoumowsky  ( Comte  de ).  Quelques 
observations  sur  les  Trilobites  et  leurs 
gisements. 

In  Annales  Sci.  Nat.  Paris,  vol.  8, 1826,  p.  186. 

Trilobites  de  Zarsko  silo. 

Remete  (A.)  Kataloge  der  Geschiebe- 
sammlung.  Berlin,  1885.  (*) 

Reuss  (A.  E.)  Entomostraca  and  Fora- 
minifera  of  the  Zechstein  of  the  Wet- 
terau.  Plate. 

In  Jahresbericht  der  wetterauischen  Gesell. 
fiir  die  gesammte  Naturk.,  1854,  p.  59  (Hanau). 

Palteontologische  Miscellen. 

In  Denkschriften  k.  Akad.  Wiss.  Wien,  vol. 
10, 1856,  7 pis. 

Lepidoderma  n.  g.,  Lepidodenna  imhoffi. 

This  genus  is  referred  by  H.  Woodward  to 
the  genus  Eurypterus. 

Reuss  (F.)  Geognostische  Bemerkungen 
auf  einer  Reise  durch  einen  Ti.eil  des 
Pilsner  Kreises. 

In  Sammlnng  naturhist.  Aufsatze,  vol.  4, 

1794,  p.  47. 


| Reuter  (G.)  Die  Beyrichien  der  obersilu- 
rischen  DiluvialgeschiebeOstpreussens. 

In  Zeitschr.  Deutsch  geol.  Gesell.,  Berlin, 
vol.  37, 1885,  p.  621,  pis.  25,  26. 

Richter  (R.)  Beitrage  zur  Palaeoutolo- 
gie  Thiiringens.  Leipzig,  1848,  6 pis. 

Aus  dern  thiiringischen  Zechstein. 

In  Zeitschr.  Deutsch.  geol.  Gesell.,  Berlin, 
vol.  7, 1855,  p.  526. 

Gythere,  Cytherella,  Cythereis,  Bairdia. 

Aus  dem  thiiringischen  Schiefe-ge- 

birge. 

In  Zeitschr.  Deutsch.  geol.  Gesell.,  Berlin, 
vol.  15, 1863,  p.  659,  2 pis. 

Harpes,  Proetus , Arethusina,  Phyllaspis  n. 
g. , Phacops,  Acidaspis,  Beyrichia. 

Aus  dem  thiiringischen  Schieferge- 

birge. 

In  Zeitschr.  Deutsch.  geol.  Gesell.,  Berlin, 
vol.  17, 1865,  p.  361,  2 pis. 

Proetus  expansus,  P.  plagiophthalmus,  Chei- 
rurus, Beyrichia  klodeni,  B.  subcylindria. 

Das  thiiringische  Schiefergebirge. 

In  Zeitschr.  Deutsch.  geol.  Gesell.,  Berlin, 
vol.  21,-1869,  p.  341. 

Proetus,  Phacops,  Dalmanites. 

Devonische  Entomostraceen  in  Thii- 

ringen. 

In  Zeitschr.  Deutsch.  geol.  Ges.ell.,  Berlin, 
vol.  21, 1869,  p.  757,  pis.  20,  21. 

Beyrichia,  Cypridina,  Cytherina. 

Roberg  (L.)  Dissertatio  academica  de 
fluviatile  Astaco,  etc.  Upsalise,  1715. 

This  work  contains  a plate  with  the  figure  of 
the  pygidia  of  Trilobites  and  a fossil  Crusta- 
cean. Fig.  H is  of  a large  pygidiuru  of  some 
species  of  Asaphus.  Fig.  J is  a cast  in  stone 
of  a smaller  species  of  the  same  genus.  The 
author  remarks  “that  he  found  the  specimens 
during  an  excursion  along  the  shores  of  the 
Baltic  Sea,  in  a red  limestone.”  He  has  the 
merit  of  referring  these  fossils  to  the  class 
Crustacea. 

Roemer  (F.  A. ) Versteinerungen  der 
Hartzgebirge.  Hannover,  1843,  12  pis. 
Crustacea,  p.  37. 

Brontes  flabellifcr,  B.  signatus,  B.  ? glabra- 
tus,  Calymene?  jo rdoni,  C.  schusteri,  C sub- 
ornatus , C.  hydrocephala,  Asaphus  zinckeni, 
Paradoxides  grotei,  Homalonotus  ahrendi,  H. 
punctatus,  H.  gigas. 

Roemer  (Ferdinand).  Beitrage  zur  ge- 
ologischen  Kenntniss  des  nordwest- 
liclien  Harzgebirges. 

In  Palajontographica,  vols.  3,  5,  and  13,  5 pts., 
Cassel,  1854-’66,  38  pis. 

Conoccphalus , Proetus,  Cyphaspis,  Phacops, 
Trimerocephalus,  Homalonotus.  Lichas,  Bron- 
teus,  Acidaspis,  Trochus,  Cheirurus , Dithyro- 
caris,  Cypridina,  Harpes,  Phillipsia. 


60 


A BIBLIOGRAPHY  OF  PALEOZOIC  CRUSTACEA. 


[bull.  63. 


Roemer  (Ferdinand)— Continued. 

Das  rheinische  Uebergangsgebirge, 

eine  palseontologisch  - geognostische 
Darstellung.  Hannover,  1844,  pi.  2. 

Phacops  latifrons,  Pleuracanthus  acimatus, 
P.  punctatus,  Gerastos  Icevigatus. 

Texas,  mit  besonderer  Riicksicht 

anf  deutscbe  Auswanderung  und  die 
pbysischen  Verhiiltnisse  des  Landes, 
nach  eigener  Beobachtung  gescbildert. 
Mit  einem  naturwissenschaftlichen 
Anbange  und  einer  topographisch- 
geognostischen  Karte  von  Texas. 
Bonn,  1849. 

In  the  list  of  fossils  on  p.  421  Pterocephalia 
sancti  sabce  Roemer  is  mentioned. 

Ueber  ein  bisher  nicbt  bescbriebenes 

Exemplar  von  Eurypterus  aus  devoni- 
scben  Schichten  des  New  York. 

In  Palaeontographica,  vol.  1,  1851,  p.  190. 

Die  Kreidebildung  von  Texas. 

Bonn,  1852,  11  pis. 

Pterocephalia  sancti  sabce  n.  g.  and  sp. 

Notiz  tiber  eine  riesenhafte  neue  Art 

der  Gattnng  Leperditia  in  silurischen 
Diluvial-Geschieben  Ost-Preussen’s. 

In  Zeitschr.  Deutsch.  geol.  Gesell , Borlin, 
vol.  10,  1858,  p.  356,  2 figs. 

Leperditia  baltica,  L.  gigantea. 

Die  Yersteinerungen  der  silurischen 

Diluvial-Geschiebe  von  Groningen  in 
Holland. 

In  Neues  Jahrbuch  fiir  Mineral.,  1858,  p.  257. 

Proetus , Encrinurus,  Beyrichia,  Cytherina. 

Die  Silurische  Fauna  des  westlichen 

Tennessee.  Breslau,  1860,  5 pis. 

Dalmania , Calymene,  Ceraurus,  Sphcerexo- 
chus,  Bumastus. 

Palseo  - lethsea.  II.  Theil:  Kohlen- 

Periode  (Silur-,  Devon-,  Kohlen-  und 
Zechstein-Formation). 

In  Bronn’s  Lethsea  geognostica,  etc.,  Stutt- 
gart, 1851-’56. 

For  list  of  genera,  see  Broun  (H.  G.)  and 
Roemer  (F.)  Lethsea  geogn. 

Bericht  Uber  eine  geologische  Reise 

nach  Norwegen  im  Sommer  1859. 

In  Zeitschr.  Deutsch.  geol.  Gesell.,  Berlin, 
vol.  11,  1860. 

Dalmania,  Cryphceus,  Asaphus,  Illcenus, 
Phacops. 

Die  fossile  Fauna  der  silurischen 

Diluvial-Geschiebe  von  Sadewitz  bei 
Oels  in  Niederschlesien.  Breslau,  1861, 
8 pis. 

Ceraurus,  Remopleurides,  Isotelus , Asaphus, 
Illcenus,  Chasmops,  Proetus , Calymene,  Encri- 
nurus,  Lichas. 


Roemer  (Ferdinand) — Continued. 

Ueber  die  Diluvial-Geschiebe  von 

nordischen  Sedimentar  - Gesteinen  in 
den  norddeutschen  Ebene  etc. 

In  Zeitschr.  Deutsch.  geol.  Gesell.,  Berlin, 
vol.  14, 1862,  p.  575. 

Beyrichia. 

Ueber  eine  marine  Conchylien-Fauna 

im  productiven  Steinkohlengebirge 
Oberschlesiens. 

In  Zeitschr.  Deutsch.  geol.  Gesell.,  Berlin, 
vol.  15,  1863,  p.  567,  pis.  14-16. 

Griffithides  mesotuberculata  McCoy,  Phillip- 
sia. 

Notiz  uber  das  Yorkommen  von 

Eurypterus  scouleri  im  niederschlesi- 
schen  Steinkohlengebirge. 

In  Zeitschr.  Deutsch.  geol.  Gesell.,  Berlin, 
vol.  25,  1873,  p.  562,  1 fig. 

Lethsea  palaeozoica.  Stuttgart,  1880. 

Text  and  atlas. 

Ueber  die  Gattung  Arthropleura  aus 

dem  schlesischen  Steinkohlengebirge. 

In  Sitzungsber.  schles.  Gesell.  fiir  vaterland. 
Cultur,  Breslau,  Jahrg.  1880,  p.  128. 

Ueber  eine  Kohlenkalk-Fauna  der 

Westkiiste  von  Sumatra.  Cassel,  1880, 
3 pis. 

Phillipsia  sumatrensis  Roemer. 

Ueber  eine  Art  der  Limuliden-Gat- 

tung  Belinurus  aus  dem  Steinkohlenge- 
birge Oberschlesien’s. 

In  Zeitschr.  Deutsch.  geol.  Gesell.,  Berlin, 
vol.  35, 1883,  p 429,  2 figs. 

Lethsea  erratica,  oder  Aufzahlung 

und  Beschreibung  der  in  den  nord- 
deutschen Ebene  vorkommenden  Di- 
luvial Geschiebe  nordischen  Sedimen- 
tar-Gesteine.  Berlin,  1885,  11  pis. 

In  this  work  many  Trilobites  and  other 
Crustacea  are  mentioned,  but  only  a few  new 
species  are  figured. 

Rogers  (\Y.  B.)  Discovery  of  Paradoxi- 
des  in  the  altered  rocks  of  Massachu- 
setts. 

In  Edinb.  New  Philos.  Jour.,  vol.  4, 1856. 

On  the  discovery  of  Cambrian  fossils 

at  Braintree,  Mass. 

In  Proc.  Boston  Soc.  Nat.  Hist.,  vol.  5, 1854, 
p.  27  (continued  on  p.  40). 

Paradoxides  harlani  Green. 

Paradoxides  near  Boston. 

In  Edinb.  New  Philos.  Jour.,  vol.  6, 1857,  p. 
314. 

Rogers  ( Henry  D.  ) The  geology  of 
Pennsylvania.  A Government  survey 
with  a general  view  of  the  geology 


V0GDE8-] 


LIST  OF  AUTHORS.  61 


Rogers  (Henry  D.) — Continued, 
of  the  United  States,  essays  on  the  coal 
formation  and  its  fossils,  and  a descrip- 
tion of  the  coal  fields  of  North  America 
and  Great  Britain.  2 vols.  Edin- 
burgh, London,  and  Philadelphia,  1858. 
Atlas  of  plates  and  maps. 

Organic  remains  of  the  Palaeozoic  strata  of 
Pennsylvania,  vol.  2,  pp.  815-834. 

Paradoxides,  Asaphus,  Calymene. 

Notes  on  the  Beyrichia  and  Leperditia,  by  T. 
Rupert  Jones,  vol.  2,  p.  834,  figs.  595-699. 

Rominger  (C.)  Description  of  Primor- 
dial fossils  from  Mount  Stephens,  N.  W. 
Territory  of  Canada. 

In  Proc.  Acad.  Nat.  Sci.  Phila.,  1887,  p.  12, 

lpl. 

Ogygia,  Embolimus  n.  g , Menocephalus, 
Conocephalites,  Bathyurus  ?,  Agnostus. 

Dr.  C.  RomingeFs  rejoinder  to  Mr. 

C.  D.  Walcott. 

In  Am.  Geologist,  vol.  2,  1888,  p.  356. 

Rouault  (Marie).  Mdmoire  sur  les  Trilo- 
bites  du  d^partement  d’llle  et-Vilaine. 

In  Bull.  Soc.  G6ol.  Prance,  2d  series,  vol.  4, 
1846,  p.  309. 

Trinucleu8,  Nileus,  Prionocheilus  n.  g.,  Caly- 
mene, Phacops,  Polyeres,  Cheirurus,  Trinucleus. 

M6moire.  1.  Sur  la  composition  du 

test  des  Trilobites.  2.  Sur  les  change- 
ments  de  formes  dus  k des  causes  acci- 
dentelles,  ce  qui  a pu  permettre  de  con- 
fondre  des  esp&ces  diffdrentes. 

In  Bull.  Soc.  G6ol.  France,  vol.  6, 1848,  p.  67, 
pis.  1-2. 

Ogygia  brongniarti,  O.  edwardsi,  Illcenus  des- 
maresti,  Calymene  arago,  Trinucleus. 

Fossiles  du  terrain  silurien,  dtage 

du  schiste,  ardoisier  fosillif&re,  Crus- 
tac6s,  famille  des  Trilobites. 

In  Bull.  Soc.  G6ol.  Prance,  vol.  8, 1851,  p.  358. 

Calymene  salteri,  O.  verneuili,  Dalmannia 
vetillarti,  D.  incerta,  Placoparia  tournemini , 
Ogygia  desmaresti,  Homalonotus  brongniarti , 
H.  barrandei,  H.  hausmanni , IT.  legraverendi, 
Plcesiacomia  kieneria,  Proetus  huhayi,  P.  mi- 
chelini,  Cyphaspis , Beyrichia,  Leperditia  n.  g., 
L.  britannica,  Phacops. 

Safford  (J.  M.)  Geology  of  Tennessee. 
Nashville,  1869,  7 pis.  and  map. 

The  author,  in  his  catalogue  of  Trenton 
and  Nashville  fossils  occurring  in  the  Central  I 
Basin,  p.  285,  gives  the  names  of  Dalmanites  j 
troosti  n.  s.  and  Encrinurus  excedrinua  n.  s.,  but 
without  specific  descriptions. 

Sandberger  (G.)  and  Sandberger  (F.)  J 
Die  Versteiueruugen  des  rheinischen  i 
Schichten -System  in  Nassau.  Wiesba-  I 
den,  1850-  56,  atlas  in  folio,  39  pis. 


Sandberger  (G  ) and  Sandberger  (F.)— 
Continued. 

Harpes,  Cyphaspis,  Trigonaspis  n.  g.,  Cylin- 
draspis  n.  g.,  Phacops,  Dalmanites,  Homalono- 
tus, Odontopleura,  Cheirurus,  Bronteus,  Cyprin- 
dia. 

Salter  (J.  W.)  On  the  structure  of  Tri- 
nucleus, with  remarks  on  other  species. 

In  Quart.  Jour.  Geol.  Soc.  London,  vol.  3, 
1847,  p.  251,  4 figs. 

Crustacea. 

In  Mem.  Geol.  Survey  Gt.  Britain,  vol.  2,  pt. 
1,  1848,  pp.  333-352,  figure,  pis.  5-8. 

Olenus , Proetus,  Phacops,  Dalmannia,  Caly- 
mene, Lichas,  Trinucleus,  Ampyx,  Ogygia,  Illce- 
nus, Acidaspis,  Cheirurus,  Sphcerexochus,  Gy- 
bele,  Agnostus,  Beyrichia. 

and  Forbes  (Edward).  Figures  and 

descriptions  illustrative  of  British  or- 
ganic remains.  Decade  2. 

In  Mem.  Geol.  Survey  United  Kingdom  Lon- 
don, 1849,  10  pis. 

Paradoxides,  Olenus,  Parabolina  n.  g.,  Pha- 
cops, Dalmannia,  Portlockia,  Cryphceus,  Caly- 
mene, Ampyx,  Brachampyx  n.  g.,  Asaphus, 
Ogygia,  Illcenus,  Bumastus. 

The  description  of  all  the  species,  with  the 
exception  of  Ampyx  nudus,  was  made  by  J.  W. 
Salter. 

Description  of  Pterygotus  problemati- 

cus  Agass. 

In  Quart.  Jour.  Geol.  Soc.  London,  vol.  8, 
1852,  p.  386,  pi.  21.  ’ 

Pterygotus,  Bellinurus. 

Appendix  A to  British  Palaeozoic 

fossils  in  the  Geological  Museum,  Uni- 
versity of  Cambridge.  London,  1852 
(Sedgwick  and  McCoy). 

Description  of  a few  species  from  Wales  and 
Westmoreland,  referred  to  in  the  foregoing 
work  by  John  William  Salter,  p.  645. 

Phacops,  Calymene,  Homalonotus,  Lichas, 
Illcenus,  Cheirurus,  Encrinurus,  Cybele,  Bey- 
richia, Cythere,  Eurypterus. 

On  the  lowest  fossiliferous  beds  of 

North  Wales. 

In  Rept.  22d  Meeting  Brit.  Assoc.  Adv.  Sci., 
1852,  Trans,  of  Sec.,  p.  56. 

Hymenocaris  n.  g. 

On  a few  genera  of  Irish  Silurian 

fossils. 

In  Rept.  22d  Meeting  Brit.  Assoc.  Adv.  Sci., 
1852,  Trans,  of  Sec.,  p.  59. 

Stygina  n.  g.,  Cyphoniscus  n.  g.,  Remopleuri- 
des,  Cyphaspis,  JEglina,  Acidaspis. 

Notes  on  the  Trilobites. 

Appendix  C to  an  article  by  Senhor  Carlos 
Ribeiro  on  the  Carboniferous  and  Silurian  for- 
mations of  the  neighborhood  of  Bussaco,  in 
Portugal. 


62 


A BIBLIOGRAPHY  OF  PALEOZOIC  CRUSTACEA. 


63. 


Salter  (J.  W.) — Continued. 

In  Quart.  Jour.  Geol.  Soc.  London,  vol.  9. 
1853,  p.  158,  pi.  7. 

Phacops,  Calymene,  Trinucleus,  Ogygia,  Illce- 
nus,  Placoparia. 


On  Arctic  Silurian  fossils. 

In  Quart.  Jour.  Geol.  Soc.  London,  vol.  9, 
853,  p.  312. 

Proetus,  Encrinurus,  Leperditia. 


Figures  and  descriptions  illustrative 

of  British  organic  remains.  Decade  7. 

In  Mem.  Geol.  Survey  United  Kingdom,  Lon- 
don, 1853,  10  pis. 

The  genera  are  arranged  in  this  work  in  the 
following  order:  1.  Phacops  downingice,  section 
Acaste,  P.  apiculatus,  P.  brongniarti,  P.  dal- 
manni , P.  jamesii,  P.  alifrons,  P.  jukesii,  P. 
conophthalmus section  Oilontochile  ( Dalman - 
nia),  P.  mucronatus,  P.  amphora.  2.  Cheirurus 
bimucronatus,  section  Crotalocephalus,  C.  arti- 
culatus?;  section  Cheirurus,  O.speciosus,  C.ge- 
lasinosus,  C.  cancrurus,  C.  octolobatus ; section 
Actinopeltis,  (7.  clavifrons.  3.  Sphcerexochus 
mirus.  4.  Encrinurus  sexcostatus,  E.  puncta- 
tus , E.  variolaris,  E.  multisegmentatus.  5. 
Cyphaspis  megalops,  C.  pygmceus  6.  Acidaspis 
jamesii,  A.  bispinosus,  A.  caractaci.  7.  Trinu- 
cleuslloydii,  section  1,  Trinucleus  proper,  T.  con- 
centricus,  with  four  varieties,  T.  thersites ; sec- 
tion 2,  Tretaspis,  T.  seticornis , T.  fimbriatus,  T. 
radiatus.  8.  R emopleurides  colbii,  R.  laterispi- 
nifer , R.  dorsopinifer section  Remopleurides, 
R.platyceps , R.  longico status,  R.  obtusus  ; sec- 
tion  2,  Caphyra , R.  (Caph.)  radians.  9.  Cypho- 
niscus  socialis.  10.  JEglina  mirabilis,  JEglina 
major. 


On  some  new  Crustacea  from  the 

uppermost  Silurian  rocks,  by  J.  W. 
Salter.  With  a note  on  the  structure 
and  affinities  of  Himantopterus,  by  T. 
H.  Huxley. 

In  Quart.  Jour.  Geol.  Soc.  London,  vol.  12, 
1856,  pi.  26,  figs.  1-7. 

Himantopterus  n.  g. 


Description  of  the  Crustaceans  from 

the  uppermost  Silurian  rocks  near  Les- 
inahago. 

In  London,  Edinb.,  Dublin  Philos  Mag.,  vol. 
11,  1856,  p.  83. 

Himantopterus. 


On  the  great  Pterygotus  (Seraphim) 

of  Scotland  and  other  species. 

In  Rept.  26th  Meeting  Brit.  Assoc.  Adv.  Sci., 
1856,  Trans,  of  Sec.,  p.  75. 


On  fossil  remains  in  the  Cambrian 

rocks  of  the  Longmynd  and  North 
Wales. 

In  Quart.  Jour.  Geol.  Soc.  London,  vol.  12, 
1856,  p.  246. 

Palceopyge  ramsayi,  pi.  4,  fig.. 3,  new  species 
and  genus. 


Salter  (J.  W.) — Continued. 

On  two  Silurian  species  of  Acidaspis 

from  Shropshire. 

In  Quart.  Jour.  Geol.  Soc.  London,  vol.  13, 
1857,  p.  210,  pi.  6. 

On  some  new  species  of  Eurypterus. 

With  note  on  the  distribution  of  the 
species. 

In  Quart.  Jour.  Geol.  Soc.  London,  vol.  15, 
1859,  p.  229,  pi.  10. 

On  the  fossils  of  the  Lingula  flags 

or  zone  Primordiale  Paradoxides  and 
Conocephalus  from  North  America. 

In  Quart.  Jour.  Geol.  Soc.  Loudon,  vol.  15, 
1859,  p.  551, 4 figs. 

Paradoxides  bennetti,  Conocephalus  antiqua- 
tus,  Asaphus  or  Olenus  sp.  ? 

New  Silurian  Crustacea. 

In  Annals  Mag.  Nat.  Hist.,  3d  series,  Lon- 
don, vol.  5, 1860,  p,  153,  figures. 

Geratiocaris , Dictyocaris  n.  g.,  Physocaris 
n.  g. 

On  the  fossils  from  the  High  Andes, 

collected  by  David  Forbes. 

In  Quart.  Jour.  Geol.  Soc.  London,  vol.  17, 
1861,  p.  62,  pis.  4,  5. 

Proetus  ( Cryphceus ) pentlandi , Homalonotus 
linares,  H.  sp.  ? , Beyrichia  forbesii,  Phacops  lati- 
frons  Bronn. 

On  some  of  the  higher  Crustacea 

from  the  British  Coal  Measures. 

In  Quart.  Jour.  Geol.  Soc.  London,  vol.  17, 
1861,  p.  528,  figs.  1-8. 

Anthrapalaemon  n.  g.,  Palceocrangon  n.  g. 

Name  changed  to  that  of  Crangopsis.  See 
same  journal,  vol.  19,  p.  80. 

Crustacea  in  the  Coal  Measures. 

In  London,  Edinb.,  Dublin  Philos.  Mag.,  vol. 
22, 1861,  p.  325. 

Anthrapalcemon. 

This  is  merely  a notice  of  the  article  referred 
to  in  the  Quart.  Jour.  Geol.  Soc.,  vol.  17, 1861,  p. 
528. 

Description  of  Uronectes  (Gamponyx) 

socialis  in  the  Rev.  T.  Brown’s  paper, 
“Mountain  limestone  and  Lower  Car- 
boniferous rocks  of  the  Fifeshire 
coast.”  (*) 

In  Trans.  Royal  Soc.  Edinb.,  vol.  22,  pt.  2, 
1861,  p.  394. 

A monograph  of  British  Trilobites. 

In  Palaeont.  Soc.  London,  vol.  16,  1862,  pp. 
1-83,  pis.  1-6,  pt.  1. 

Phacops,  subgenera  Trimerocephalus  McCoy , 
Phacops  Emm. , Acaste  Gold.,  Ohasmops  McCoy, 
Odontochile  Corda,  Cryphceus  Green. 

Cheirurus,  subgenera  Crotalocephalus  Sal- 
ter, Oheirurus  Beyrich,  Eccoptochile  Corda, 
Actinopeltis  Corda,  Sphcerexochus  Beyrich, 

Amphion  Pander. 


V0GDE8.] 


LIST  OF  AUTHORS, 


63 


Salter  (J.  W.)— < Continued. 

On  some  fossil  Crustacea  from  tlie 

Coal  Measures  and  Devonian  rocks  of 
New  Brunswick,  Nova  Scotia,  and  Cape 
Breton. 

In  London,  Edinb.,  Dublin  Philos.  Mag.,  4th 
series,  vol.  24, 1862,  p.  166. 

A monograph  of  British  Trilobites. 

Pt.  2.  Pp.  81-128,  pis.  7-19. 

In  Palaeont.  Soc.  London,  vol.  17,  1863. 

Calymene,  Momalonotus,  subgenera  Bron- 
gniartia  Salter  (not  Brongniartia  Eaton),  Tri- 
merus  Green,  Dipleura  Green,  Koenigia  Salter, 
Burmeisteria  Salter;  Ogygia,  Staurocephalus, 
Deiphon,  Amphion. 

On  some  fossil  Crustacea  from  the 

Coal  Measures  and  Devonian  rocks  of 
British  North  America. 

In  Quart.  Jour.  Geol.  Soc.  London,  vol.  19, 
1863,  p.  75,  figs.  1-12. 

Amphipeltis  n.  g.,  Diplostylus  n.  g.,  Eurypte- 
rus, Palceocrangon. 

The  author  herein  changes  the  name  Palceo- 
crangon Salter  to  that  of  Crangopsis. 

On  some  species  of  Eurypterus  and 

allied  forms. 

In  Quart.  Jour.  Geol.  Soc.  London,  vol.  19, 
1863,  p.  81,  8 wood-cuts. 

Eurypterus  scouleri,  E.  (Arthropleura?) 
mammatus,  E.  ? (Arthropleura)  ferox. 

On  Peltocaris,  a new  genus  of  Silu- 
rian Crustacea. 

In  Quart.  Jour.  Geol.  Soc.  London,  vol.  19, 
1863,  p.  87. 

Peltocaris  n.  g.,  Hymenocaris,  Geratiocaris, 
Dictyocaris,  Dithyrocaris,  Arges,  Apus,  Nebalia, 
Estheria,  Leperditia,  Beyrichia. 

On  some  tracks  of  Lower  Silurian 

Crustacea. 

In  Quart.  Jour.  Geol.  Soc.  London,  vol.  19, 
1863,  p.  92,  figures. 

Note  on  the  Skiddaw  slate  fossils. 

In  Quart.  Jour.  Geol.  Soc.  London,  vol.  19, 
1863,  p.  135,  figures. 

Caryocaris  n.  g. 

On  the  discovery  of  Paradoxides  in 

Britain. 

In  Quart.  Jour.  Geol.  Soc.  London,  vol.  19, 
1863,  p.  274. 

Paradoxides  davidis. 

On  a new  Crustacean  from  Glasgow 

Coal  Field. 

In  Quart.  Jour.  Geol.  Soc.  London,  vol.  19, 
1863,  p.  519,  figs.  1,  2. 

Palceocarabus  russellianus. 

A monograph  of  British  Trilobites. 

Pt.  3.  Pp.  129-179,  pis.  15-25. 

In  Palmont.  Soc.  London,  vol.  18,  for  1864 
(London,  1866). 


Salter  (J.  W.) — Continued. 

Ogygia , subgenera  Barrandia,  and  Homalop- 
teon  ; Niobe , Asaphus,  subgenera  Ptychopyge, 
Basilicus,  Mcgalaspis,  Isotelus,  Cryptonymus, 
Symphysurus,  Brachyaspis,  and  Nileus ; Sty- 
gina,  Psilocephalus  n.  g. 

Figures  and  descriptions  illustrative 

of  British  orgauic  remains.  Decade  XI. 
Trilobites  (chiefly  Silurian). 

In  Mem.  Geol.  Survey  United  Kingdom,  Lon- 
don, 1864,  10  pis. 

Paradoxides , Angelina , Olenus,  O.  ( Lepto - 
plastus),  O.  ( Peltura ),  O.  ( Splicer ophthalmus), 
O.  ( Parabolina ),  Conocoryphe,  Phacops  (Tri- 
merocephalus),  Salteria  n.  g.,  Stygina,  Asaphus, 
JEglina,  Staurocephalus , Agnostus,  A.  ( Condy - 
lopyge),  A.  (Trinodus),  A.  (Phalacroma). 

The  article  on  Salteria  primceva  n.  g.  et  sp., 
pi.  6,  was  edited  by  P.  Wj ville  Thomson. 

On  some  fossils  from  the  Lingula 

flags  of  Wales. 

In  Quart.  Jour.  Geol.  Soc.  London.,  vol.  20, 
1864,  p.  233,  pi.  13. 

Paradoxides,  Anopolenus  n.  g.,  Conocoryphe, 
Holocephalina  n.  g.,  Microdiscus,  Agnostus, 
Leperditia . 

Note  on  the  fossils  from  the  Budleigh 

Sandstone  Pebble  bed. 

In  Quart.  Jour.  Geol.  Soc.  London,  vol.  20, 
1864,  p.  286,  pi.  15. 

Phacops  incertus,  Calymene  tristani,  Soma- 
lonotus  brongniarti,  Myocaris  n.  g. 

For  detailed  description  of  Myocaris,  see 
Geol.  Mag.,  vol.  1,  London,  1864,  p.  11,  fig. 4. 

On  the  new  genus  Anopolenus. 

In  Geol.  Mag.,  vol.  1,  London,  1864,  p.  6. 

Anopolenus  n.  g.,  Myocaris. 

Catalogue  of  the  Museum  of  Practi- 
cal Geology  of  London.  London,  1865. 

and  Woodward  (Henry).  Chart 

of  fossil  Crustacea,  accompanied  by  a 
descriptive  catalogue  of  all  the  genera 
and  species  figured.  London,  1865, 
pis.  3 and  4. 

Permian : Prosopiniscus,  Dcdmanites  ? ka- 
bliktce,  Estheria,  Kirkbya,  Bairdia,  Cythcrideis, 
Cythere,  Limulus. 

Coal : Palceocarabus,  Pygocephalus,  TJronectus 
(Gampsonyx),  Diplostylus,  Phillipsia,  Estheria, 
Beyrichia,  Kirkbya,  Leperditia,  Oandona,  Leaia, 
Arthropleura,  Eurypterus,  Limulus ? (Bclinu- 
rus). 

Mountain  Limestone:  Palceocrangon , Brachy- 
metopus,  Grijffithides,  Phillipsia,  Dithyrocaris, 
Cyclus,  Estheria,  Cythere,  Gypridina,  Cyprella, 
Cypridella,  Entomoconchus,  Beyrichia,  Bairdia, 
Leperditia,  Eurypterus,  Limulus  1 trilobitoides. 

Devonian  : Amphipeltis,  Gilocrangon,  Campe- 
caris,  Proetus,  Encrinurus,  Bronteus,  Phacops, 
Oyphaspis,  Arges,  Typhomiscus,  Uomalonotus, 
JIarpes,  Cypridina,  Esther  ia,  Leperditia,  Ento - 


64 


A BIBLIOGRAPHY  OF  PALEOZOIC  CRUSTACEA. 


[uull.  63. 


Salter  (J.  W.)— Continued. 

mis,  Gypridina,  Beyrichia,  Bostrichopus , Eu- 
rypterus,  Pterygotus. 

Upper  Silurian:  Bronteus,  lllcenus,  Cyphas- 
pis,  Proetus,  Aulacopleura,  Phacops,  Encri- 
nurus,  Acidaspis,  Cheirurus,  Homalonotus,  Dei- 
phon,  Calymene,  Harpes,  Dictyocaris,  Beyrichia , 
Ceratiocaris,  Leperditia,  Stylonurus,  Pterygotus, 
Hemiaspis,  Slimonia,  Bunodes. 

Lower  Silurian:  Asaphus,  Stygina,  Nileus , 
lllcenus,  AEglina,  Ogygia,  Agnostus,  Niobe,  Pha- 
cops, Trinucleus,  Ampyx,  Sphcerexochus , Dio- 
nide,  Eccoptochile,  Placoparia,  Lichas,  Oybele , 
Acidaspis,  Calymene,  Staurocephalus,  Jtemo- 
pleurides,  Gyphoniscus,  Atops,  Triarthrus,  Gory 
nexochus,  Centropleura,  Monocephalus,  Pelto- 
caris,  Beyrichia,  Cytheropsis,  Protichnites. 

Cambrian : Agnostus,  Sao,  Anomocaris,  Doli- 
chometopus,  Anpocaris,  Solenopleura,  Eliipso- 
cephalxbs , Arionellus,  Conocoryphe,  Olenus,  Ace- 
rocaris,  Hydrocephalus,  Paradoxides,  Loncho- 
cephalus,  Dikelocephalus,  Palceopyge. 

See  also  Kept.  35th  Meeting  Brit.  Assoc.  Adv. 
Sci.,  1865,  Trans,  of  Sec.,  p.  79 ; Geol.  Mag.,  vol. 

2,  London,  1865,  p.  468. 

and  Blanford  (H.  F. ) Palaeontology 

of  Nib,  in  the  northern  Himalayas. 
Calcutta,  1865. 

On  some  additional  fossils  from  the 

Lingula  flags,  with  a note  on  the  genus 
Anopolenus , by  Henry  Hicks. 

In  Quart.  Jour.  Geol.  Soc.  London,  vol.  21, 
1865,  p.  476. 

Anopolenus,  Conocoryphe,  Microdiscus,  Holo- 
cephalina,  Agnostus,  Erinnus  n.  g. 

On  the  fossils  of  North  Wales. 

In  Mem.  Geol.  Survey  Gt.  Brit.,  vol.  3,  Lon- 
don, 1866,  p.  239,  37  pis. 

Dikelocephalus,  Olenus,  Parabolina,  Conoco- 
ryphe, Angelina,  Homalonotus.  Lichas,  Trinu- 
cleus, Dionide,  Ampyx,  Asaphus,  Niobe,  JEglina, 
Cheirurus,  Encrinurus,  lllcenus,  Agnostus,  Psi- 
locephalus,  Beyrichia,  Hymenocaris. 

A monograph  of  British  Trilobites. 

Pt.  4.  Pp.  177-216,  pis.  25-30. 

In  Palaeont.  Soc.,  vol.  20,  1867. 

Ogygia,  Barrandia,  lllcenus,  subgenera  Oc-  I 
tillcenus,  Panderia,  Dysplanus,  lllcenus,  Ectil-  | 
Icenus,  Hydrolcenus,  Illcenopsis,  and  Bumastus.  \ 
Family  Bronteidce. 

A monograph  of  British  Trilobites. 

This  work  forms  different  parts  of  the  Palae-  ! 
ont.  Soc.  London,  volumes  for  1862-’67,  as  sepa- 
rately itemized  in  this  connection. 

On  Saccocaris  major. 

In  Kept.  Proc.  Geol.  Poly  tech.  Soc.  West  Rid- 
ing of  Yorkshire  (for  1867),  vol.  4,  1868,  p.  588. 

and  Hicks  (Henry).  On  some  fos- 
sils from  the  Menevian  group. 

In  Quart.  Jour.  Geol,  Soc.  London,  vol.  25, 
J869,  p.  51,  pis.  2,  3. 


Salter  (J.  W.) — Continued. 

Paradoxides,  Plutonia  n.  g.,  Conocoryphe. 

In  a note  on  p.  52,  Mr.  J.  W.  Salter  suggests 
the  new  generic  name  of  Plutonia,  but  leaves 
the  description  for  another  article. 

A species  of  this  genus  was  afterwards  de- 
scribed and  figured  in  the  same  journal,  vol.  27, 
1871,  p.  299,  pi.  15,  figs.  1-8,  under  the  name  of 
Plutonia  sedgwicki  Hicks.  This  large  species 
has  affinities  with  the  genera  Paradoxides  and 
Anopolenus  in  the  form  of  its  glabella,  but  dif- 
fers, according  to  Hicks,  “in  having  the  whole 
surface  covered  with  coarse  tubercles  or 
spines.”  The  term  Plutonia  is  objectionable, 
inasmuch  as  it  was  used  in  1864  for  a genus  of 
the  Mollusca. 

Catalogue  of  the  collection  of  Cam- 
brian and  Silurian  fossils  contained  in 
the  Geological  Museum  of  the  Univer- 
sity of  Cambridge,  1873. 

and  Etheridge  (R.)  On  the  fossils 

of  North  Wales. 

In  Geology  of  North  W ales,  with  an  appendix 
on  the  fossils  by  J.  W.  Salter,  revised  and  added 
to  by  K.  Etheridge ; Mem.  Geol.  Survey  Gt. 
Brit.,  vol.  3,  London,  1881,  2d  ed.,  623  pp.,  113 
illustrations,  2 geol.  maps,  26  plates  of  fossils. 

Paradoxides,  Plutonia,  Anopolenus,  Dikelo- 
cephalus, Olenus,  j ( Sphcerophthalmus ),  Cono- 
coryphe, Angelina,  Arionellus,  Phacops,  Caly- 
mene, Homalonotus , Lichas,  Trinucleus,  Ampyx, 
Dionidce,  JEglina,  Asaphus,  Ogygia , Barrandia, 
Niobe,  lllcenus,  Illcenopsis,  Cheirurus,  Placo- 
paria, Encrinurus,  Cybele,  Agnostus , Microdis- 
cus, Carausia,  Holocephalina,  Nesuretus,  Psilo- 
cephalus,  Hymenocaris,  Lingulocaris,  Ceratio- 
caris, Entomis,  Beyrichia,  Leperditia. 

Monograph  of  British  Trilobites  from 

the  Cambrian,  Silurian,  and  Devonian 
formations.  Pt.  5. 

Palaeont.  Soc.  London,  vol.  37,  1883,  pp.  215, 
and  index,  3 figs. 

lllcenus  bowmanni?,  I.  crassicauda,  I.  ( Bu- 
mastus) sp.  ? 

See  Huxley  (T.  H.)  and  Salter  (J. 

W.).  Also  Salter  (J.  W.)  and  Sharpe 
(D.). 

Sars  (M.)  Ueber  einige  neue  oder  un- 
vollstaudig  bekannte  Trilobiten. 

In  Isis  (oder  Encycl.  Zeitung),  Oken,  1833, 
p.  33. 

Scheuchzer  ( J.  J.)  Specimen lithologim 
Helvetia.  Turici,  8vo,  1702.  (*) 

Metoorologia  et  Orytographia  Hel- 
vetica, oder  Beschreibung  der  Luftge- 
schichten,  Steinen,  Metallen,  etc.  Tu- 

| rici,  1718.  (*) 


VOGDES.  J 


LIST  OF  AUTHORS, 


G5 


Schlotheim  (E.  Fr.  von).  Beschreibuug 
einer  seltenen  Trilobiten-Art. 

In  Taschenbuch  fiir  gesam.  Mineral.,  Leon- 
hard, 1810,  pi.  1,  figs.  1-6. 

Trilobiten  cornigerus  Schloth. 

Nachtrage  zur  Petrefactenkunde. 

11.  Gotba,  1823,  pi.  22. 

1.  Trilobites  blumenbachii,  2.  T.  tristani , 3.  T. 
variolatus , 4.  T.  macrophthalmus,  5.  T.  sulzeri, 

6.  T.  hoffi,  7.  T.  cornigerus , 8.  T.  de  buchii,  9.  T. 
hausmani , 10.  T.  schroet,  11.  T.  caudatus,  12.  T. 
laticauda,  13.  T.  guettardi,  14.  T.  desmarestii, 
15.  T.  tessini,  16.  T.  spinulosus,  17.  T.  scara- 
boides,  18.  T.  gibbosus,  19.  T.  laciniatus , 20.  T. 
sphcerocephalus,  21.  T.  pisiformis,  22.  T.  granu- 
latu8,  23.  T.  punctatus,  24.  T.  mucronatus,  25. 

T.  bucephalus , 26.  T.  crassicauda,  27.  T.  tenta- 
culatus,  28.  T.  problematicus,  29.  T.bitumenosus. 

Beschreibuug  eiuiger  abgebildeteu 

Arten  von  Echinosphseriten  und  Tri- 
lobiten. o 

In  Isis  (oder  Encycl.  Zeitung),  Oken,  1826,  p. 
309,  pi.  1,  figs.  8, 9 ; also  F6russ.,  Bull.,  1827,  vol. 

12,  p.  406. 

Tril.  esmarcki , T.  granum  ( Agnostus ). 

Schmid  (E.  E.)  Die  kleineren  organi- 
schen  Formen  des  Zechsteinkalkes  von 
Setters  in  der  Wetterau. 

In  Neues  Jahrbuch  fiir  Mineral.,  1867,  p. 
676,  plate. 

Cy  there. 

Schmidt  ( Fr.  ) Untersuckungen  iiber 
die  silurische  Formation  von  Ehstland, 
Nord-Livland  und  Oesel. 

In  Archiv  Naturk.  Liv-,  Ehst-  u.  Kurl., 
Dorpat,  vol.  2,  1858-59,  pp.  443,  445,  448,  453, 
461,  463. 

Miscellanae  Silurica.  I.  Ueber  die 

russischen  silurischen  Leperditien  mit 
Hinznziehung  einiger  Arten  aus  den 
Nachbarlandern. 

In  M6ua.  Acad.  Imp.  Sci.  St.-P6tersbourg,vol. 
21,  No.  2, 1873, 1 pi. 

Leperditia,  Isochilina. 

Einige  Bemerkungen  iiber  die  po- 

dolisch-galizische  Silurformation  und 
deren  Petrefacten.  St.  Petersburg, 
1875,  1 pi. 

Proetus,  CyphaspU,  Phacops,  Oalymene,  En- 
crinurus,  Sphcerexochus,  lllcenus  ( Bumastus ), 
Leperditia , Eurypterus,  Pterygotus. 

Revision  der  ost-baltischen  siluri 

schen  Trilobiten,  nebst  geognostischer 
Uebersicht  des  ost-baltischen  Silurgo- 
biets. 

In  M6m.  Acad.  Imp.  Sci.  St.-P6tersbourg,  vol. 
30,  No.  1, 1881, 16  pis. 

Phacopid®,  genera,  Phacopx.  Acaste,  Ptcrygo-  | 
metopus  u.  g.,  Ohasmops.  Cheirurida1.,  genera,  ! 
Cheirums,  Cyrtometopus,  tiphcercxochus,  Pscu-  | 

Bull.  G3 5 


Schmidt  (Fr.)— Continued. 

dosphoerexochus  n.  g.,  Nieszkowskia  n.  g.,  Am- 
phion,  Diaphanometopus  n.  g.,  Encrinurid® 
Cybele,  Encrinurus. 

and  Jones  (T.  Rupert).  On  some 

Silurian  Leperditia. 

In  Annals  Nat.  Hist.,  4th  series,  vol.  9,  Lon- 
don, 1882,  p.  168. 

Miscellanae  Silurica.  III.  1.  Nach- 

trag  zur  Monographie  der  russischen 
silurischen  Leperditien.  2.  Die  Crus- 
taceenfauna  der  Eurypterenschichten 
von  Rootzikiill  auf  Oesel. 

In  M6m.  Acad.  Imp.  Sci.  St.-P6tersbourg,vol. 
31,  No.  5, 1883,  9 pis. 

Leperditia,  Bunodes,  Pseudoniscus,  Eurypte- 
rus, Pterygotus , Geratocaris. 

and  Jones  (T.  Rupert).  See  Jones 

(T.  Rupert)  and  Schmidt  (Fr.). 

Ueber  einige  neue  ostsibirische 

Trilobiten  und  verwandte  Thierformen. 

In  Bull.  Acad.  Sci.  Imp.  St.-P6tersbourg,  vol. 
30,  No.  4, 1886,  p.  502. 

Agnostus,  Phacops , Proetus,  Oyphaspis,  Eu- 
rypterus. 

Schrenk  (G.  A.)  Uebersicht  des  obern- 
silurischen  Schichten-Systems  Liv-  und 
Ehstlands,  etc. 

In  Archiv  Naturk.  Liv-,  Ehst-  u.  Kurl., 
Dorpat,  vol.  1854,  pp.  35  and  86. 

Leperditia. 

Scouler  (John).  Description  of  a fossil 
crustaceous  animal.  (*) 

In  Edinb.  Jour.  Nat.  Geogr.  Sci.,  Vol.  3, 1831, 
p.  352,  pi.  10. 

The  author  describes  in  this  article,  under 
the  new  generic  name  of  Eidothea,  certain  frag- 
ments of  an  Eurypterus. 

Account  of  some  fossil  Crustacea 

which  occur  in  the  coal  formation 
( Argas ). 

In  Record  of  Geol.  Sci.  (Thomson’s),  vol.  1, 
1835,  p.  136. 

According  to  Capt.  J.  E.  Portlock  (Rept. 
Geol.  Londonderry,  etc.,  1843,  p.  313),  “ Dr.  John 
Scouler  first  noticed  this  remarkable  Crusta- 
cean found  by  him  in  the  Carboniferous  strata 
of  Paisley;  and  depending  as  a principal  charac- 
ter on  the  lateral  caudal  appendages,  he  pointed 
out  its  analogy  to  the  genera  Cyclops  and  Apus; 
and  again,  at  the  meeting  of  the  British  Associa- 
tion at  Glasgow,  he  described  two  species,  one 
of  which,  Argas  tricornis,  in  all  probability  de- 
pends on  an  illusive  appearance  produced  by  tho 
overlapping  of  the  crust  of  different  individuals. 
* * * I)r.  John  Scouler  having  subsequently  al- 
tered his  view  of  the  affinities  of  the  genus,  ho 
now  considers  it  a bi-valved  Crustacean,  dis- 
tinguished by  not  being  able  to  retract  tho  tail 
within  tho  shell,  and  hence  has  named  it  Dilhy- 


66 


A BIBLIOGRAPHY  OF  PALEOZOIC  CRUSTACEA. 


[bull.  63. 


Scouler  (John)— Continued. 

rocaris,  or  bivalved  shrimp,  abandoning  the 
original  name  as  one  already  pre-occupied.” 

TheRept.  10th Meeting  Brit.  Assoc.  Adv.  Sci., 
1840,  held  at  Glasgow,  does  not  contain  in  the 
index  Dr.  iScotiler’s  name  or  that  of  the  genus 
Argos  or  Dithyrocaris.  In  the  5th  Kept,  of  the 
“Committee  on  the  Fossil  Phyllopoda  of  the  Pa- 
laeozoic Rocks,”  1887,  the  genus  Dithyrocaris 
Scouler  is  quoted  on  the  authority  of  Captain 
Portlock  as  follows : “ Dithyrocaris  Scouler  in 
Portlock’s  Geol.  Report,  Londonderry,  etc., 
1843,”  p.  313. 

Scudder  (Samuel  H.)  Ehachura,  a new 
genus  of  fossil  Crustacea. 

In  Proc.  Boston  Soc.  Hat.  Hist.,  vol.  19, 1878, 
p.  296,  pi.  9,  figs.  3,  3 a. 

In  the  5th  Rept.  to  the  Brit.  Assoc.  Adv. 
Sci.,  1887,  on  the  fossil  Phyllopoda  by  the  com- 
mittee, consisting  of  Mr.  R.  Etheridge,  Dr.  H. 
Woodward,  and  Prof.  T.  Rupert  Jones  this 
new  genus  of  S.  H.  Scudder  is  referred  to  as 
probably  of  that  of  Dithyrocaris  Scouler,  1843. 

Shaler  (N.  S.)  and  Foerste  (A.  F.)  Pre- 
liminary description  of  North  Attle- 
borough fossils. 

In  Bull.  t>Iu8.  Comp.  Zool.  Harvard  Coll., 
vol.  16,  Ho.  2, 1888,  Geol.  Series,  vol.  2, 1888,  p.  27, 
2 pis. 

Paradoxides,  Ptychoparia,  Microdiscus. 

Sharpe  (Daniel).  On  the  geology  of 
the  neighborhood  of  Oporto,  including 
the  Silurian,  coal,  and  slates  of  Val- 
longo. 

In  Quart.  Jour.  Geol.  Soc.  London,  vol.  5, 
1849,  p.  142.pl.  6. 

Isotclus  powissii  Port.,  Illcenus  lusitanicus 

Sharpe. 

Description  of  the  new  species  of 

Zoophyta  and  Mollusca.  Appendix  B 
to  an  article  on  the  Carboniferous  and 
Silurian  formations  of  the  neighbor- 
hood of  Bussaco,  in  Portugal,  by  C. 
Ribeiro. 

In  Quart.  Jour.  Geol.  Soc.  London,  vol.  9, 
1853,  p.  146. 

Dithyrocaris?  longicauda  Sharpe. 

Shumard  (B.  F.)  Palaeontology.  Crus- 
tacea. 

In  1st  and  2d  Ann.  Repts.  of  the  Geol.  Survey 
of  Missouri  (Swallow),  1855,  pt.  2,  p.  195,  pi.  B. 

Proetus , Gyphaspis,  Phillipsia,  Dalmania , 
Calymene,  Acidaspis,  Encrinurus,  Cythere. 

Notice  of  new  fossils  from  the  Per- 
mian strata  of  New  Mexico  and  Texas, 
collected  by  Dr.  George  G.  Shumard, 
geologist  of  the  U.  S.  Government  ex- 
pedition for  obtaining  water  by  means 
of  artesian  wells  along  the  32d  parallel, 


Shumard  (B.  F.)— Continued, 
under  the  direction  of  Capt.  John  Pope, 
U.  S.  Corps  of  Top.  Eng. 

Trans.  Acad.  Sci.  St.  Louis,  vol.  1, 1858,  p.  290. 

Phillipsia  perannulata,  pi.  11,  fig.  10. 

The  Primordial  zone  of  Texas,  with 

descriptions  of  new  fossils. 

In  Am.  Jour.  Sci.,  2d  series,  vol.  32,  1861,  p. 
213. 

Dikelocephalus,  Conocephalites,  ArioneUus , 
Agnostus. 

Notice  of  some  new  and  imperfectly 

known  fossils  from  the  Primordial 
zone  (Potsdam  sandstone  and  calcif- 
erous  sand  group)  of  Wisconsin  and 
Missouri. 

In  Trans.  Acad.  Sci.  St.  Louis,  vol.  2, 1863,  p. 

101. 

Dikelocephalus , Arionellus,  Conocephalites, 
Agnostus. 

Descriptions  of  new  Palaeozoic  fos- 
sils. 

In  Trans.  Acad.  Sci.  St.  Louis,  vol.  2, 1863,  p. 
108. 

Proetus  proutii. 

Sjogren  (A.)  Anteckningar  om  Oland, 
ett  bidrag  till  Sveriges  geologi. 

In  Ofversigt  K.  Vet.-Akad.  Forhandl.  Stock- 
holm, vol.  8, 1851,  Ho.  2,  p.  36. 

Enumerates  species  of  the  following  genera: 
Pemopleurides , Paradoxides,  Ellipsocephalus, 
Olenus,  Phacops,  Calymene,  H omalonotus,  Li- 
chas,  Ampyx,  Cheirurus,  Asaphus,  Illcenus, 
Nileus,  Battue,  Cytherina. 

Om  nagra  forsteningar  i Olands 

Kambriska  lager. 

In  Geol.  Foreningens  Stockholm  Forhandl., 
vol.  1,  Ho.  5, 1871, 1 pi. 

Paradoxides,  Ellipsocephalus , Conocoryphe, 
Agnostus. 

Sowerby  (J.  D.  C.)  Description  of  Ho- 
malonotus  knighti  in  Adam  Sedgwick 
and  R.  I.  Murchison’s  article  on  the 
older  formation  on  the  right  bank  of 
the  Rhine,  etc. 

In  Trans.  Geol.  Soc.  London,  2d  series,  vol.  6, 
1842,  p.  275,  figure,  pi.  38,  fig.  17. 

Stainer  (X.)  Note  sur  un  Trilobite  nou- 
veau. 

In  Annales  Soc.  G6ol.  Belgique ; M6moires, 
vol.  14,  1887. 

Dechenella. 

Steinhart  (E.  T.  G.)  Die  bis  jetat  in 
preuss.  Geschieben  gefundenen  Trilo- 
biten. 

In  Beitrage  zur  Hatur.  Preuss.,  herausge- 
geben  von  der  phys.  - okonomischen  Gesell., 
Konigsberg,  1874. 


VOGDES.} 


LIST  OF  AUTHORS. 


G7 


Steinhart  (E.  T.  G.) — Continued. 

Harpes,  Proetus,  Cyphaspis,  Phacops,  C ha- 
mops,  Galymene,  Dalmania,  Licha,  Ampyx , 
Asaphus , A.  ( Basilicus ),  Illcenus , Nileus , jBw- 
mastus,  Acidaspis,  Ceraurus,  Sphcerexochus , 
Zethus,  Encrinurus,  Aynostus. 

Steininger  (Jean).  Observations  sur  les 
fossiles  du  calcaire  interm^diaire  de 
l’Eifel. 

In  M6m.  Soc.  G6ol.  France,  vol.  1, 1831,  p.  331, 

pL  21. 

Galymene  brongniarti,  G.  latreilii,  G.  schlot- 
heimii,  C.  tristani,  Proetus  n.  g.,  P.  cuvieri, 
Olenus  punctatus,  Asaphus  mucronati,  A.lati- 
cauda. 

Sternberg  (Kasper  Graf  von).  Ueber- 
sicht  der  in  Bohmen  dermalen  bekann- 
ten  Trilobiten. 

In  Yerhandl.  mineral.  Gesell.  vaterlandisch. 
Mus.  Bohm.,  1825,  p.  69,  pis.  2,  3;  Isis  (oder 
Encycl.  Zeitnng),  Oken,  vol.  7,  1827,  p.  627. 

Trilobites  macrophthalmus,  T.  hausmanni,  T. 
sulzeri,  T.  hoffii,  T.  tessini. 

Ueber  die  Gliederung  und  die  Ftisse 

der  Trilobiten. 

In  Isis  (oder  Encycl.  Zeitung),  Oken,  1830, 
pp.  516,  563,  pi.  5,  figs.  1-3. 

Ueber  bbhmische  Trilobiten. 

In  Yerhandl.  mineral.  Gesell.  vaterlandisch. 
Mus.  Bohm.,  1833,  p.  17. 

Olenus  longicaudatus,  Trilobites  spinosus, 
Olenus  pyramidalis,  O.  latus,  Conoceph.  costa- 
tus, Trilobites  sulzeri,  T.  zippii,  Ellipsocephalus 
ambigus,  Trilobites  hojji,  Otarion  diffractum, 
Trilobites  sternbergi,  T.  ungula,  T.  or natus. 

Ueber  die  bohmischen  Trilobiten  mit 

Beziehung  auf  die  Arbeiten  von  Boeck  1 
nnd  Zenker  dariiber. 

In  Neues  Jahrbuch  fur  Mineral.,  1835,  p.  727. 

Olertus  longicaudatus,  O.  latus,  Trilobites 
minor,  T.  gracilus,  T.  sulzeri,  T.  hoffi,  T.  stern- 
bergi, T.  angula,  T.  ornatus,  T.  gibbosus,  Otarion 
diffractum. 

Steschegloff.  Treatise  on  the  Trilobites 
of  Petersburg.  (*) 

In  Jour,  fur  neue  Entdeckungen  in  der 
Phys  , Chera.,  Natur.,  und  Technologic,  St.  Pe- 
tersburg, Jibs.  1,  2,  1827,  pi.  8.  (In  Russian.) 

Deucalion  n.  g. 

Stock  (Thomas).  Note  on  the  occur- 
rence of  Anthrapalcemon  etheridgi  B.  N. 
Peach,  in  the  ironstones  above  the 
sandstones  at  Craigleith  Quarry,  near 
Edinburgh. 

In  Trans.  Edinb.  Geol.  Soc.,  vol.  4, 1881,  p.  97. 

Note  on  the  occurrence  of  the  re- 
mains of  Decapod  Crustaceans  in  the 

Wardie  shales. 


Stock  (Thomas) — Continued. 

In  Trans.  Edinb.  Geol.  Soc.,  vol.  4,  1882,  p. 
219. 

Palceocrangon,  Anthrapalcemon. 

Stoddart  (W.  W.)  On  Trilobites. 

In  Proc.  Bristol  Nat.  Sei.,  vol.  1, 1866,  p.  82. 

Stokes  (Charles).  On  a Trilobite  from 
Lake  Huron. 

In  Trans.  Geol.  Soc.  London,  2d  series,  vol. 
1, 1822,  p.  208,  pi.  28. 

Strauss-Durckheim  (H.)  Ueber  Estlie - 
via  dahalacensis  Riiffell,  eine  neue  Gat- 
tung  aus  der  Familie  der  Daphniden. 

In  Mus.  Senckenberg:anum,  vol.  2,  1837,  pp. 
119-128,  pis.  7,  7 b. 

The  name  Estheria  was  originally  proposed 
by  Dr.  Ruffell  for  a species  brought  from  Abys- 
sinia; its  description,  with  figures  of  typical 
species,  appeared  in  the  above  cited  work.  In 
the  same  year  Mr  Audouin  (Annales  Soc.  En- 
tom.,  vol.  6)  proposed  that  of  Gyzicus  for  simi- 
lar species,  without  a generic  description.  The 
simultaneous  publication  of  these  two  generic 
names  for  the  same  genus  lead  Mr.  Joly  (An- 
nales Sci.  Nat.,  2d  series,  vol.  17,  1842,  p.293)  to 
propose  that  of  Isaura.  Estheria  is  now  gene- 
rally used  by  authors. 

Symonds  (W.  S.)  On  a Phyllopod  Crus- 
tacean in  the  Upper  Ludlow  rock  of 
Ludlow. 

In  Kept.  25th  Meeting  Brit.  Assoc.  Adv.  Sci., 
1855,  Trans,  of  Sec.,  p.  98. 

Hymenocaris  vermicauda. 

On  a new  species  of  Eurgpterus  from 

the  Old  Red  Sandstone  of  Hereford- 
shire. 

In  Kept.  27th  Meeting  Brit.  Assoc.  Adv.  Sci., 
1857,  Trans,  of  Sec.,  p.  93. 

On  a new  species  of  Eurgptems  from 

the  Old  Red  Sandstone  of  Hereford- 
shire. 

In  Edinburgh  New  Philos.  Jour.,  vol.  6, 1857, 
p.  257. 

Tate  (George).  Fame  Islands. 

In  Proc.  Berwickshire  Nat.  Club,  vol.  3,  No. 
7,  p.  222. 

Griffithides  farnensis. 

Thomson  (P.  Wyvillo).  Oil  some  spe- 
cies of  Acidaspis  from  the  Lower  Silu- 
rian beds  of  the  south  of  Scotland. 

In  Quart.  Jour.  Geol.  Soc.  London,  vol.  13, 
1857,  p.  206,  pi.  6. 

Figures  and  descriptions  illustra- 
tive of  organic  remains. 

In  Geol.  Survey  United  Kingdom,  decade  XI, 
London,  1864,  pi.  6. 

Salter ia  primes va  Wyv.  Thomson  n.  g.  and 
sp. 


68 


A BIBLIOGRAPHY  OF  PALEOZOIC  CRUSTACEA. 


[BULL.  63. 


Tietze  ( E.  ) Ueber  die  devonischen 
Schichten  von  Ebersdorf  unweit  Neu 
rode  in  der  Grafschaft  Glatz. 

In  Geognostisch  - palseont.  Monographic, 
Stuttgart,  1870,  2 pis. 

Harpes , Proetus,  Phacops,  Cypridina. 

Todd  (J.  E.)  A description  of  some  fos- 
sil tracks  from  the  Potsdam  sandstone. 

In  Trans.  Wisconsin  Acad.  Sci.,  vol.  5,  1882, 
p.  276, 1 fig. 

Tornquist  ( S.  L.  ) Om  lagerfoljden  i 
Dalarnes  under-Siluris  <a  bildningar. 

In  Lunds  TJniv.  Arsskrift,  vol.  3,  1867. 

Berattelse  om  en  geologisk  resa 

genom  Skanes  och  Ostergotlands  pa- 
leozoiska  trakter  sommaren  1875,  etc. 

In  Ofversigt  Kongl.  Svenska  Yet.  Akad. 
Forhandl.,  18:5,  No.  10,  p.  43. 

Paradoxides,  Olenus,  Phacops,  Calymene , 
Asaphus,  Illcenus , Trinucleus,  Lichas , Agnos • 
tus. 

Undersokningar  bfver  Siljansomra- 

dets  Trilobitfauna. 

In  Svenska  Geol.  IJndersdkning,  Stockholm, 
series  C,  No.  66, 1884,  2 pis. 

Harpes,  Pemopleurides,  Triarthrus,  Proelus, 
Gyphaspis , Arethusina,  Isoielus,  Phacops,  Pha- 
cops ( Pterygometopus ),  Phacops  ( Ghasmops ), 
Calymene,  Romalonotus,  Lichas,  Trinucleus, 
Ampyx,  Deiphon,  Asaphus,  Megalaspis,  Niobe, 
Acidaspis,  Cheirurus,  Sphcerexochus , Cyrtome- 
topus,  PseudosphcerexocMis , Nieszlcowskia , Sphce- 
rexocoryphe,  Pliomera,  Encrinurus,  Cybele, 
Bronteus,  Illcenus,  Nileus,  Agnostus.  Telephus. 

Torrubia  (J.)  Aparato  para  la  historia 
natural  espanola.  Yol.  1.  Madrid, 
1754,  p.  83,  par.  13,  No.  96. 

The  Rev.  Father  Joseph  Torrubia  has  the 
merit  of  referring  the  Trilobites  to  the  class 
Crustacea. 

Traquair  (R.  H.)  Occurrence  of  Trilo- 
bites in  the  Carboniferous  limestone  of 
Fifeshire.  (*) 

In  Proc.  Royal  Phys.  Soc.  Edinburgh,  vol.  2, 
1858-’61 , p.  253. 

On  the  Grijffithides  mucronatus  Mc- 
Coy. 

In  Jour.  Royal  Geol.  Soc.  Ireland,  vol.  2, 1869, 
p.  213,  plate. 

Trautschold  (H.)  Die  Trilobiten  als 
Erstgeborene. 

In  Bull.  Soc.  Imp.  des  Naturalistes,  Moscou, 
1872,  p.  297. 

Die  Kalkbruche  von  Mjatschkowa. 

Eine  Monographie  des  oberen  Berg- 
kalkes. 

In  M6m.  Soc.  Imp.  des  Naturalistes,  Moscou, 
vol.  13,  1874,  p.  276. 


Trautschold  (H.)— Continued. 

Phillipsia  globiceps,  P.  grunswaldti,  P.pustu • 
lata. 

Trenkner  (M.  W.)  Paloeontolog.  Novi- 
taten  vom  nordwestl.  Harze.  Halle, 
1367-’69,  8 pis. 

Harpes,  Gyphaspis,  Bronteus,  Entomis. 

Tristan  (J.)  Sur  un  crustac6  renfermd 
dans  quelques  schistes,  notamment  dans 
ceux  des  environs  de  Nantes  (d6pt.  de 
la  Loire-Inf4rieure)  et  d’ Angers  (ddpt. 
de  Maine-et-Loire). 

In  Jour.  Mines,  vol.  23,  1808,  p.  2. 

( Calymene  tristani  Brong.) 

Tromelin  (G.)  andLebesconte  (P.)  Ob- 
servations sur  les  terrains  primaires  du 
nord  du  d6pt.  d’llle-et-Vilaine  et  de 
quelques  autres  parties  du  massif  bre- 
ton. 

In  Bull.  Soc.  Geol.  France,  3d  series,  vol.  4, 
1875-76,  p.  583. 

Dalmanites,  Calymene,  Homalonotus,  Trinu- 
cleus. 

Tschernyschew.  Die  Fauna  des  mittl. 
und  oberen  Devon  am  Westabhange 
des  Urals. 

In  Mem.  du  Comit6  G6ol.,  vol.  3,  No.  3, 1887, 
p.  14. 

Dechenella. 

Tullberg  (S.  A.)  Om  ^ywosfws-arterna  i 
de  Kambriska  aflagringame  vid  Andra- 
rum. 

In  Svenska  Geol.  Undersok.,  series  C,  No.  42, 
1882,  2 pis. 

Ulrich  (E.  O.)  Description  of  some  spe- 
cies of  fossils  from  the  Cincinnati  group. 

In  Jour.  Cincinnati  Soc.  Nat.  Hist.,  vol.  1, 
1878-79,  p.  92. 

Trinucleus  bellulus. 

Description  of  a Trilobite  from  the 

Niagara  group  of  Indiana. 

In  Jour.  Cincinnati  Soc.  Nat.  Hist.,  vol.  2, 
1879,  p.  131,  3 figs. 

Calymene  nasuta. 

Descriptions  of  new  genera  and  spe- 
cies from  the  Lower  Silurian  about  Cin- 
cinnati. 

In  Jour.  Cincinnati  Soc.  Nat.  Hist.,  vol.  2, 
1879,  p.  8,  pi.  9. 

Beyrichia,  Leperditia. 

Verneuil  (Edouard).  Sur  les  fossiles  d6- 
voniens  des  environs  de  Sabers  dans  les 
montagnes  de  L6on. 

In  Bull.  Soc.  G6ol.  France,  2d  series,  vol.  7, 
1850,  p.  155,  pi.  3. 

Cryphceus  calliteles,  Phacops  lati/rons,  1 roma- 
lonotus pradianus. 


VOGDES.] 


LIST  OF  AUTHORS. 


69 


Verneuil  (Rdouard) — Continued. 

Geologic  de  la  Russie  d’Europe  et 

des  montagnes  de  l’Oural,  par  R.  I. 
Murchison,  Edouard  de  Verneuil  et  le 
cointe  Alex,  de  Keyserling.  Vol.  2.  3 

part.  Palajontologie.  Londres  et  Paris, 
1845,  50  pis. 

Calymene  odini , C.  fischeri,  Asaphus  expan- 
sue,  Phillipsia  eichwaldi,  P.  ouralica  n.  s. 

and  Barrande  (Joachim).  Descrip- 
tion des  fossiles  trou\6s  dans  les  ter- 
rains silurien  et  devonien  d’Almaden 
d'une  partie  de  la  Sierra  Morena  et  des 
montagnes  de  Tobide. 

In  Bull.  Soc.  G6ol.  France,  2d  series,  vol.  12, 
1854-’55,  p.  904,  pis.  23, 24. 

Ellipsocephalus  pradoanus,  Calymene  pul- 
chra,  C.  tristani,  C.  arago,  C.  transienus,  Homa- 
lonotus  rarus , H.  brongniarti,  Placoparia  tour- 
neminei,  Dalmanites  socialis,  D.  dujardini,  D. 
vetillarti,  D.  torrubice,  D.  phillipsi,  D.  downin- 
gice,  Lichas  hispanica,  Tiinucleus  gold/ussi, 
Cheirurus  marianus,  Asaphus  nobilis,  A.  cianus, 
A.  glabratus,  A.  contractus , Illcenus  hispanicus , 
1.  sanchezi,  Ogygia. 

Sur  Fexistence  de  la  faune  pri- 

mordiale  dans  la  chalne  Cantabrigue, 
par  M.  C.  de  Prado,  suivie  de  la  de- 
scription des  fossiles  par  MM.  de 
Verneuil  et  Barrande. 

InBulL  Soc.  G6oL  France,  2d  series,  vol.  13, 
1860,  p.  5.6,  pis.  6-8. 

Paradoxides,  Conocephalites,  Arionellus,  Ag- 
nosias. 

and  d’Archiac.  ( Vicomte .)  Paldon- 

tologie  sur  la  faune  d6vonienne  des 
rives  du  Bosphore.  Liste  des  fossiles 
recueillis  par  Abdullah-Bey. 

In  Comptes  Rendus  Acad.  Sci.,  Paris,  1867,  p. 
1217. 

Note  sur  les  fossiles  recueillis  en 

1863  par  M.  de  Tchihatchef  aux  envi- 
rons de  Constantinople. 

In  Boll.  Soc.  G6oL  France,  vol.  21,  1864,  p.  147. 
Homalonotus,  Cheirurus. 

Verworm  (M. ) Zur  Entwicklungsge- 
schichte  der  Beynchieu. 

In  Zeitscbr.  Deutsch.  geol.  Gesell.  Berlin, 
vol.  39, 1887,  p.  27. 

Vine  (G.  R.)  Notes  on  the  distribution 
of  the  Entomostraca  in  the  Wenlock 
shales. 

In  Proc.  Yorkshire  Geol.  Polytechnic  Soc.,  1 
vol. 9,  pt. 3, 1887-88, p.  393. 

Vitry  (Abbdde).  M&noire  sur  les  fossiles 
du  Tournaisds  et  les  purifications  en 
g6n6ral,  relativement  a lour  utility 
pour  la  vie  civile. 


Vitry  (Abbd  de) — Continued. 

In  M6m.  Acad.  Roy  ale  Sci.,  Bruxelles,  vol.  3, 
1780,  p.  15,  pi.  1,  fig.  1 ( Phillipsia ) ; pi.  3,  figs.  9-11. 
Vogdes  (A.  W.)  Notes  on  the  genera 
Acidaspis,  Odontopleura,  and  Cerato- 
cephala,  etc. 

In  Proc.  Acad.  Nat.  Sci.,  1877,  p.  138. 

Short  notes  on  the  geology  of  Ca- 
toosa County,  Georgia. 

In  Am.  Jour.  Sci.,  3d  series,  vol.  23,  1879,  p. 
475. 

Calymene  rostrata  n.  s. 

Description  of  a new  Crustacean 

from  the  Upper  Silurian  of  Georgia, 
with  remarks  on  Calymene  elintoni. 

In  Proc.  Acad.  Nat.  Sci.  Phila.,  1880,  p.  176, 4 
figs. 

Calymene  rostrata,  C.  elintoni. 

Fig.  3,  Calymene  elintoni,  has  been  referred 
by  A.  F.  Foerste  (Bull.  Den.  Univ.,  vol.  2, 1887, 
p.  95,  pi.  8,  figs.  12, 16)  to  Calymene  vogdesi. 

A new  Trilobite. 

In  12th  Ann.  Rept.  Geol.  Nat.  Hist.  Survey 
Minnesota,  1884,  p.  8. 

Bathyurus  stonemani  n.  s. 

Description  of  a new  Crustacean 

from  the  Clinton  group  of  Georgia,  with 
remarks  upon  others.  New  York  City, 
1886,  5 pp.,  4 figs. 

Encrinurus  americanus  n.  s.,  Calymene  ros- 
trata, and  C.  elintoni. 

The  genera  and  species  of  North 

American  Carboniferous  Trilobites. 

In  Annals  New  York  Acad.  Sci.,  vol.  4, 1887, 
p.  69, 2 pis. 

Proetus,  Phillipsia,  Griffithides,  Brachymeto- 
pu8. 

Description  of  two  new  species  of 

Carboniferous  Trilobites. 

In  Trans.  New  York  Acad.  Sci.,  vol.  7,  1888, 
p.  247, 1 wood-cut. 

Phillipsia,  Griffithides  ? 

Volborth  (A.)  Ueber  einige  russische 
Trilobiten. 

In  Yerhandl.  tubs.  k.  mineral.  Gesell.  zu  St. 
Petersburg,  1847,  p.  1,  pi.  1. 

Tho  author  redescribed  the  genus  Zethus 
Pander  and  its  type  Zethus  verrucosus,  placing 
Cybele  bellatulus  Eichw.  under  the  same  genus. 

Ueber  das  Prioritiitsrecht  der  Trilo  • 

biten-Gattung  Zethus  Pander  gegen  die 
Gattuug  Cryptonymu8  Eichwald. 

In  Bull.  Physico-Math.  Acad.  Sci.,  St.-P6ters- 
bourg,  1854,  p.  251. 

Ueber  die  Bewegungs-Organe  der 

Trilobiten.  Folgendes  mit. 

In  Verhaudl.  russ.  k.  mineral.  Gesellsch.zn 
St.  Petersburg,  1857— ’58,  p.  168. 


70  A BIBLIOGRAPHY  OF  PALEOZOIC  CRUSTACEA.  [bull.  63. 


Volborth  (A.)— Continued. 

Ueber  die  Crotaluren  und  Remopleu- 

riden,  ein  Beitrag  zur  Kenntniss  der 
russischen  Trilobiten. 

In  Yerhandl.  rass.  k.  mineral.  Gesell.  zu  St. 
Petersburg,  1857-58,  p.  126,  pi.  13. 

Crotalurus  n.  g.,  Remopleurides. 

Ueber  die  mit  glatten  Rumpfglie- 

dern  versehenen  russischen  Trilobiten, 
nebst  einem  Anhange  liber  Bewegungs- 
organe  und  fiber  das  Herz  derselben. 

In  M6m.  Acad.  Imp.  Sci.  St.-P6tersbourg, 
vol.  6,  No.  2, 1863, 48  pp.,  4 pis. 

lllcenus,  Dysplanus,  Panderia  n.  g.,  Nileus, 
Bumastus. 

Ueber  einige  neue  ehstlandische 

Illsenen . 

In  M6tn.  Acad.  Imp.  Sci.  St.-P6tersbourg, 
vol.  8,  No.  9, 1864,  2 pis. 

Ueber  Herrn  von  Eicliwald’s  Beitrag 

zur  naheren  Kenntniss  derlllaenen,  etc. 

In  Bull.  Soc.  Imp.  des  Naturalistes,  Moscou, 
1866,  No.  1,  p.  77. 

Wahlenberg  (Geo.)  Petrificata  telluris 
Suecana!'  Upsaliae,  1818. 

Tbis  work  was  published  and  distributed  in 
1818  as  a separate  article,  in  advance  of  the 
Nova  Acta  Reg.  Soc.  Sci.,  vol.  8, 1821. 

Petrificata  telluris  Suecana  exami- 

nata  a Georgio  Wahlenberg. 

In  Nova  Acta  Reg.  Soc.  Sci.,  Upsal.,  vol.  8, 
1821,  pp.  1-116,  pis.  1-4. 

Entomostracites  expansus  Linn.,  E.  crassicau- 
da n.  s.,  E.  laticauda  n.  s.,  E.  caudatus  Brim.,  E. 
granulatus  n.  s.,  E-  tuberculatus  Brim.,  E.punc- 
tatus  Brum,  E.  laciniatus  n.  s.,  E.  paradozissi- 
mus  Linn.  ( Paradoxides  tessini),  E.  bucephalus 
(hypostoma  of  P.  tessini ),  E.  spinulosa  n.  s.,  E. 
gibbosus  n.  s.,  E.  scaraboeoides  n.  s.,  E.  pisi- 
f or  mis  Linn. 

Additamenta  qusedam  ad  petrificata 

telluris  Suecana. 

In  Nova  Acta  Reg.  Soc.  Sci.,  Upsal.,  vol.  8, 
1821,  pp.  293-296,  pi.  7. 

Entomostracites  crassicauda,  E.  expansus , E. 
tuberculatus , E.  caudatus , E.  laticauda. 

Entomostracites  crassicauda , pi.  7,  fig.  5,  has 
been  referred  by  G.  Holm.  (De  Svenska  Ar- 
terna  Trilobitslagetet  lllcenus,  1882,  p.  55)  to 
lllcenus  esmarkii  Sclilotheim. 

Walch  (J.  E.  T.)  Des  Trilobites  dans 
le  rbgne  des  purifications,  ou  de  la 
conque  rid6e  a trois  lobes  (concha 
triloba  rugosa).  Recueil  des  monu- 
meus  des  catastrophes  que  le  globe  de 
la  terre  a essui6es,  contenaut  despfitri- 
fications.  (Knorr,  G.  W.)  Vol.  3.  Nu- 
remberg, 1775,  p.  105. 


Walch  (J.  E.  T.) — Continued. 

See  also  voL  2,  1768,  section  1,  p.  81 ; vol.  3, 
1775,  pp.  184,  185, 186, 193  ; suppl.  pis.  8,  9 a,  9 b, 
9 c,  9 e,  9 f.  German  and  French  editions. 

This  author  gives  the  name  of  Trilobite  to 
the  family,  a designation  which  has  been  used 
by  all  subsequent  authors,  with  the  exceptions 
of  J.  W.  Dalman  and  C.  S.  Rafinesque. 

Walcott  (C.  D.)  Description  of  a new 
species  of  Trilobite  [from  Trenton  Falls, 
New  York.] 

In  Cincinnati  Quart.  Jour.  Sci.,  vol.  2, 1875,  p. 
273, 2 figs. 

Sphcerocoryphe  robustus. 

New  species  of  Trilobite  from  the 

Trenton  limestone  at  Trenton  Falls, 
N.  Y. 

In  Cincinnati  Quart.  Jour.  Sci.,  vol.  2, 1875,  p. 
347,  wood-cuts. 

Remopleurides  striatulus. 

Notes  on  Ceraurus  pleurexanthemus 

Green. 

In  Annals  Lyceum  Nat.  Hist.,  New  York, 
vol.  11, 1876,  p.  155,  pi.  11. 

Preliminary  notice  of  the  discovery 

of  the  remains  of  the  natatory  and 
branchial  appendages  of  Tiilobites. 

In  28th  Rept.  New  York  State  Mus.  Nat. 
Hist.,  1875,  p.  89. 

Description  of  new  species  of  fossils 

from  the  Trenton  limestone. 

In  28th  Rept.  New  York  State  Mus.  Nat. 
Hist.,  1875,  p.  93. 

Bathyurus,  Asaphus. 

Notes  on  some  sections  of  Trilobites 

from  the  Trenton  limestone. 

In  31st  Rept.  New  York  State  Mus.  Nat. 
Hist.,  1879,  p.  61.  Advanced  sheets  published 
September  20,  1877, 1 pi. 

Notes  upon  the  legs  of  Trilobites. 

In  31st  Rept.  New  York  State  Mus.  Nat. 
Hist.,  1879,  p.  64. 

Notes  upon  the  eggs  of  the  Trilobites. 

In  31st  Rept.  New  York  State  Mus.  Nat. 
Hist.,  1879,  p.  66.  Advanced  sheets  published 
September  20,  1877. 

Descriptions  of  new  species  of  fos- 
sils from  the  Chazy  and  Trenton  lime- 
stones. 

In  31st  Rept.  New  York  State  Mus.  Nat. 
Hist.,  1879,  p.  69.  Advanced  sheets  published 
September  20,  1877. 

Arionellus,  Dcdmanites , Asaphus,  Addaspis, 
Ceraurus,  Encrinurus,  lllcenus. 

The  Utica  slate  and  related  forma- 
tions of  the  same  geological  horizon. 

In  Trans.  Albany  Inst.,  vol.  10,  1879,  p.  2, 
pis.  1,  2. 


V0GDES.  J 


LIST  OF  AUTHORS. 


71 


Walcott  (C.D.) — Continued. 

Metamorphoses  of  Triarthrus  becJci. 

Triarthrus  becki  and  JBeyriehia  Cincinnati- 
ensis. 

Description  of  new  species  of  fossils 

from  the  Carboniferous  formation. 

In  32d  Rept.  New  York  State  Cab.  Nat.  Hist., 
1879,  p.  129.  Pamphlet  published  in  advance  of 
the  report 

Conocephalites,  Ptychaspis,  Bathyurus. 

The  Trilobite,  new  and  old  evidence 

relating  to  its  organization. 

In  Mus.  Comp.  Zool.  Harvard  Coll.,  vol.  8, 
1881,  p.  191,  6 pis. 

Description  of  a new  genus  of  the 

order  Eurypterus  from  the  Utica  slate. 

In  Am.  Jour.  Sci.,  3d  series,  vol.  23,  1882,  p. 
213,  figures. 

Echinognathus  n.  g. 

Description  of  new  species  of  fossils 

from  the  Trenton  group,  New  York. 

In  35th  Kept.  Hew  York  State  Cab.  Hat. 
Hist.,  1883,  p.  206, 1 pi. 

Beyrichia,  Leper ditia  (Tsochilina) . 

Author’s  edition,  October  15, 1883, 8 pp.,  1 pi. 

Injury  sustained  by  the  eye  of  a 

Trilobite  at  the  time  of  moulting  of  the 
shell. 

In  Annals  Hat.  Hist , 5th  series,  vol.  13,  Lon- 
don, 1884,  p.  69. 

On  the  locomotory  appendages  of 

Trilobites. 

In  Science,  vol.  3, 1884,  p.  279, 3 figs. 

Asaphus  megistos,  Calymene  senaria. 

Palaeontology  of  the  Eureka  district. 

In  Mon.  H.  S.  Geol.  Survey,  vol.  8, 1884,  24  pis. 

JHcellocephalus,  Olenellus,  Ptychoparia,  P. 

( Solenopleura ),  P.  (Pterocephalus) , Anomocare, 
Bathyurus , Chariocephalus,  Ptychaspis , Agrau- 
los,  Proetus,  Cyphaspis,  Arethusina,  Phillipsia, 
Grifjithides,  Phacops,  Dalmanites,  Trinucleus , 
Asaphus,  Symphysurus , Ogygia?,  Barrandia? , 
lllcenurus,  Ceraurus,  Amphion,  Illcenus,  Agnos- 
tus,  Leperditia,  Beyrichia , Primitia,  Plumulites. 

On  the  Cambrian  faunas  of  North 

America.  Preliminary  studies. 

In  Bull.  H.  S.  Geol.  Survey,  No.  10,  1884, 
10  pis. 

Paradoxides,  Conocoryphe,  Harttia  n.  g.,  Pty- 
choparia, Agno8tu8,  Microdiscus,  Agraulos,  Pro- 

tocaris  n.  g. 

Palaeozoic  notes : New  genus  of  Cam- 
brian Trilobites,  Mesonacis. 

In  Am.  Jour.  Sci.,  3d  series,  vol.  29, 1885,  p. 
328,  figures. 

Describes  a new  genus,  Mesonacis,  and  sub- 
stitutes the  generic  name  Bailiella  of  Matthew 
for  the  subgenus  & ' alter m,  proposed  by  him  j 
(Bull.  U.  S.  Geol.  Survty,  Ho.  10,  lt84). 


Walcott  (C.  D.) — Continued. 

Second  contribution  to  the  studies 

on  the  Cambrian  fauna  of  North  Amer- 
ica. 

In  Bull.  U.  S.  Geol.  Survey,  Ho.  30, 1886. 

Figures  and  descriptions  of  species  of  the  fol- 
lowing genera  are  given,  viz : Paradoxides , Ba- 
thynotus,  Mesonacis,  Olenellus,  Olenoides,  Oryc- 
tocephalus  n.  g , Ptychoparia,  Solenopleura, 
Anomocare,  Grepicephalus,  Dorypyge,  Asaphis- 
cus,  Bathyuriscus,  Agnostus , Microdiscus,  Proty- 
pus  n.  g.,  Protocaris,  Leperditia. 

Fauna  of  the  upper  Taconic  of  Em- 
mons, in  Washington  County,  New 
York,  with  one  plate. 

In  Am.  Jour.  Sci.,  3d  series,  vol.  34,  1887,  p. 
187. 

Solenopleura  ?,  Ptychoparia  ?,  Microdiscus, 
Olenoides,  Conocoryphe,  Aristozoe,  Leperditia. 

Cambrian  fossils  from  Mount  Ste- 
phens, North  West  Territory  of  Canada. 

Am.  Jour.  Sci.,  3d  series,  vol.  36,  1888,  p.  161. 

Ptychoparia,  Agnostus,  Bathyuriscus,  Olenoi- 
des, Zacanthoides  n.  g. 

Stratigraphic  position  of  the  Olenel- 
lus fauna  in  North  America  and  Eu- 
rope. 

Am.  Jour.  Sci.,  3d  series,  vol.  37,  1889,  p.  374. 

Leperditia,  Aristozoa,  Protocaris,  Agnostus , 
Microdiscus,  Olenellus,  Paradoxides , Olenoides, 
Zacanthoides,  Bathynotus,  Avalonian,  g.,  Cono- 
coryphe, Ptychoparia,  Agraulos,  Grepicephalus, 
Oryctocephalus,  Anomocare,  Protypus,  Soleno- 
pleura. 

Waldschmidt  (E.)  Ueber  die  devoni- 
schen  Schichten  der  Gegend  von  Wild- 

ungen. 

In  Zeitschr.  Deutsch.  geol.  Gesell.,  vol.  37, 
1885,  p.  906,  pis.  37-40. 

Phacops,  Bronteus,  Cypridina. 

Warder  (John  A.)  New  Trilobites. 

In  Am.  Jour.  Sci.,  1st  series,  vol.  34,  1838,  p. 
377. 

Geratocephala  n.  g. 

This  article  on  the  new  genus  Geratocephala 
was  read  before  the  Western  Academy  of  Sci- 
ence, May  25, 1838. 

Washburn  (W.  T.)  The  geology  of  the 
Bosphorus. 

In  Am.  Jour.  Sci.,  3d  series,  vol.  6, 1873,  p.  186. 

Hot  descriptive ; contains  important  notes  on 
fossil  Crustacea. 

Weitenweber  (W.  R.)  Systematisches 
Verzeichniss  der  bohmischen  Trilobiten 
in  der  Sammlung  des  Dr.  Zeidler. 

In  Lotos,  vol.  7, 1847,  pp.  5-42. 

Wetherby  (A.  G.)  Description  of  a new 
family  and  genus  of  Lower  Silurian 
Crustacea. 


I BULL.  63. 


72  A BIBLIOGRAPHY  OF  PALEOZOIC  CRUSTACEA. 


Wetherby  (A.  G.) — Continued. 

In  Jour.  Cincinnati  Soc.  Nat.  Hist.,  vol.  1, 
1878-79,  p.  162,  figure,  vol.  2,  pi.  7,  figs.  1,  1 a^g. 
Enoploura  balanoides. 


White  (C.  A.)  and  St.  John  (O.  H.)— 
Continued. 

Calymene  senaria,  Cyphaspis  christyi,  Phil- 
lipsia  bufo. 


Description  of  new  fossils  from  the 

Lower  Silurian  and  Subcarboniferous 
rocks  of  Ohio  and  Kentucky. 

In  Jour.  Cincinnati  Soc.  Nat.  Hist.,  vol.  4,  1 
1881,  p.  77. 

Proetus,  Isochilina. 

White  (C.  A.)  and  St.  John  (O.  H.)  Pre- 
liminary notice  of  new  genera  and 
species  of  fossils.  Iowa  City,  May  8,  j 
1867, 3 pp. 

Beyrichia  lithof actor,  B.  lithof actor  var.  velata,  j 
Oythere  simplex. 

Of  this  small  pamphlet  only  fifty  copies  were 
published  by  the  Iowa  State  Geological  Sur-  j 
vey.  Republished  in  Trans.  Chicago  Acad,  j 
Sci.,  vol.  1, 1867. 

Description  of  new  subcarbon-  ] 

iferous  and  Coal-Measure  fossils  col- 
lected upon  the  geological  survey  of 
Iowa,  together  with  a notice  of  new 
generic  characters  observed  in  two 
species  of  Brachiopods. 

In  Trans.  Chicago  Acad.  Sci.,  vol.  1,  pt.  1,  I 
1867,  p.  115,  2 figs. 

Beyrichia  petrifactor,  B.  petrifactor  var. 
velata,  B.  foetoidea,  Cythere  simplex. 

In  this  article  the  authors  give  the  new 
names  of  Beyrichia  petrifactor  to  the  species 
described  in  the  preliminary  notice  as  B.  litho-  j 
factor,  and  also  change  the  name  of  B.  litho-  I 
factor  var.  velata  to  that  of  Beyrichia  petrifactor  j 
var.  velata. 

Preliminary  report  upon  inverte- 
brate fossils  collected  by  the  expedi- 
tions of  1871,  1872,  and  1873,  with  de-  i 
scriptions  of  new  species. 

In  Geog.  and  Geol.  Expl.  Surveys  West  100th  j 
Meridian,  Washington,  1874. 

Olenellus,  Dicellocephalus,  Megalaspis,  Ag- 
nostus,  Leperditia. 

Report  upon  the  invertebrate  fossils 

collected  in  portions  of  Nevada,  Utah, 
Colorado,  New  Mexico,  and  Arizona,  by 
parties  of  the  expeditions  of  1871,  1872, 
1873,  and  1874. 

In  Geographical  Surveys  West  100th  Meri- 
dian, Palaeontology,  vol.  4,  1877,  pt.  1,  pp.  1-219, 
pis.  1-21. 

Olenellus,  Dicellocephalus , Asaphiscus,  Cono- 
coryphe  ( Ptychoparia ),  Megalaspis,  Agnostus, 
Leperditia. 

Palaeontology  : Fossils  of  the  Indiana 

rocks. 

In  2d  Ann.  Rept.  Dept.  Statistics  and  Ge-  | 
ology,  Indiana,  1880,  pp.  471-522,  pis.  1-11. 


The  fossils  of  the  Indiana  rocks. 

No.  3. 

In  13th  Ann.  Rept.  Dept.  Geol.  and  Nat.  Hist. 
Indiana,  1883,  pt.  2,  pp.  107-180,  pis.  23-39. 

Phillipsia  (Griffithides?)  scitala,  P.  ( G . ?)  san- 
gamonensis,  Eurypterus  ( Anthraconetes ) mazo- 
nensis,  Anthrapalcemon  gracilis,  Acanthotelson 
stimpsoni,  A.  eveni , Palceocaris  typus,  Dithyro- 
caris  carbonarius,  Leaia  tricarinata,  Euproops 
dance,  E.  colletti. 

Whiteaves  (J.  F. ) Palfeozoic  fossils. 
Yol.  3,  pt.  1,  1884. 

In  Geol.  and  Nat.  Hist.  Survey  Canada,  1884, 
8 pis. 

Eurypterus  boylei. 

Contributions  to  Canadian  palaeon- 
tology. Yol.  1. 

In  Geol.  and  Nat.  Hist.  Survey  Canada,  1888. 

In  the  author’s  list  of  fossils  from  the  Hamil- 
ton formation  of  Ontario  the  following  Crus- 
tacea are  included:  Phacops  bufo , Dalmanites 
helena,  D.  boothii,  and  Cythere  ? ( Beyrichia ) 
punctulifera. 

. See  Matthew  (G.  F.)  Illustra- 
tions of  the  fauna  of  the  St.  John 
group.  No.  3. 

In  Trans.  Royal  Soc.  Canada,  vol.  3,  1885, 
p.  76. 

Solenopleura  acadia  Whiteaves. 

Whitfield  (R.  P.)  Description  of  new 
species  of  fossils. 

In  Rept.  Reconnoissance  from  Carrol,  Mon- 
tana Territory,  on  the  Upper  Missouri,  to  the 
Yellowstone  National  Park  and  return,  Lud- 
low’s report,  Washington,  1876. 

Crepicephalus  ( Loganellus ) montanensis, 
Arionellus  tripunctatus. 

See,  also,  Rept.  Chief  Eng.  U.  S.  A.,  1876, 
Appendix  NN. 

Preliminary  descriptions  of  new 

species  of  fossils  from  the  lower  geo- 
logical formation  of  Wisconsin. 

In  Ann.  Rept.  Geol.  Survey  Wisconsin,  1877, 
pp.  50-89. 

Dicellocephalus,  ConocephaXites,  Ptychaspis, 
Crepicephalus,  Agraulus  ( Bathyurusf ),  Arionel- 
lus, Ellipsocephdlus,  Illcenurus,  Bronteus. 

Preliminary  report  on  the  palaeon- 
tology of  the  Black  Hills,  containing 
descriptions  of  new  species  of  fossils 
from  the  Potsdam,  Jurassic,  and  Creta- 
ceous formations  of  the  Black  Hills  of 
Dakota. 

In  U.  S.  Geol.  Survey  Rocky  Mountain  Re- 
gion, Washington,  1877. 

Crepicephalus  (Loganellus)  centralis , C.  (Lo- 
ganellus) planus. 


VOGDES.] 


LIST  OF  AUTHORS. 


73 


Whitfield  (R.  P. )— Continued. 

Description  of  new  species  of  fossils 

from  the  Palaeozoic  formations  of  Wis- 
consin. 

In  Ann.  Rept.  Geol.  Survey  Wisconsin,  1879, 
• pp.  44-71. 

DiceUocephalus,  Orepicephalus  ? , Ptychaspis, 
Aglaspis,  Conocephalites  ? , Conocephalites  (Pty- 
chaspis ?),  Asaphus,  Illcenus. 

New  forms  of'  fossil  Crustaceans 

from  the  Upper  Devonian  rocks  of 
Ohio,  with  descriptions  of  new  genera 
and  species. 

In  Am.  Jour.  Sci.,  3d  series,  vol.  19, 1880,  p.  33. 

Echinocaris  n.  g.,  Palceopalcemon  n.  g. 

A plate  and  explanation  accompany  the 
author’s  edition. 

Palaeontology  of  the  Black  Hills  of 

Dakota. 

In  U.  S.  Geog.  and  Geol.  Survey  Rocky 
Mountain  Region.  Rept.  Geol.  and  Resources 
of  the  Black  Hills  of  Dakota,  with  atlas ; by 
Henry  Newton  and  Walter  Jenney,  Washing- 
ton, 1880,  p.  325,  pi.  2. 

Orepicephalus  planus,  O.  centralis. 

Palaeontology. 

In  GeoL  Wisconsin,  vol.  4,  1882,  pt.  3,  pp.  163- 
363,  pis.  1-27. 

DikeUocephalus,  Conocephalites , O.  ( Ptychas- 
pis?),  Ellipsocephalu8,  Orepicephalus,  Ptychas- 
pis, Arionellus,  A.  ( Agraulos ),  Agraulos  (Bathy- 
urus?),  Aglaspis,  I llcenur us,  Asaphus,  Illcenus, 
Sphcerexochus,  Phacops,  Bronteus,  Leperditia. 

Description  of  new  species  of  fossils 

from  Ohio,  with  remarks  on  some  of  the 
geological  formations  in  which  they 
occur. 

In  Annals  New  York  Acad.  Sci.,  vol.  2,  Nos. 
7,  8, 1882,  p.  193. 

Eurypterus,  Leperditia,  Plumulites. 

. On  the  fauna  of  the  Lower  Carbonif- 

erous limestones  of  Spergen  Hill,  Indi- 
ana, with  a revision  of  the  descriptions 
of  its  fossils  heretofore  published,  and 
illustrations  of  the  species  from  the 
original  type  series. 

In  Ball.  Am.  Mus.  Nat.  Hist.  New  York,  vol. 
1,  No.  3, 1882,  pi.  9. 

Leperditia  carbonaria  Hall,  Oytherellina  glan- 
della  n.  s. 

Plates  republished  in  12th  Rept.  Geol.  Nat. 
Hist.  Indiana,  1882. 

List  of  Wisconsin  fossils. 

In  GeoL  Wisconsin,  vol.  1,  1883,  p.  362;  also 
illustrations  of  typical  fossils  of  the  Wisconsin 

formations. 

Notice  of  some  new  species  of  Pri- 
mordial fossils  in  the  collection  of  the 


Whitfield  (R.  P.) — Continued. 

Museum,  and  corrections  of  previously 
described  species. 

In  Bull.  Am.  Mus.  Nat.  Hist.,  New  York,  vol. 
1,  No.  5, 1884,  p.  139,  pis.  14, 15. 

DikeUocephalus,  Olenellus,  Arionellus,  Oono- 
cephalites , Angelina. 

Notice  of  a very  large  species  of 

Homalonotus  from  the  Oriskany  sand- 
stone formation. 

In  Bull.  Am.  Mus.  Nat.  Hist.,  New  York,  vol. 
1,  No.  6, 1885,  p.  193,  pi.  22. 

Homalonotus  major  Whitfield. 

Notice  of  geological  investigations 

along  the  eastern  shore  of  Lake  Cham- 
plain, conducted  by  Prof.  H.  M.  Seely 
and  Prest.  Ezra  Brainerd,  of  Middle- 
bury  College,  with  descriptions  of  the 
new  fossils  discovered. 

In  Bull.  Am.  Mus.  Nat.  Hist.,  New  York,,  vol. 

1,  No.  8, 1886,  p.  293. 

Saof  lamottensis  n.  s.,  Lichas  champlainensis 
n.  8.,  Asaphus  canalis  Conrad. 

Observations  on  some  imperfectly 

known  fossils  from  the  calciferous 
sandrock  of  Lake  Champlain,  and  de- 
scriptions of  several  new  forms. 

InBull.  Am.  Mus.  Nat.  Hist.,  New  York,  vol. 

2,  No.  2, 1889,  p.  41, 13  pis. 

Primitia  gregaria,  P.  ? cristata,  P.  seelyi, 
Bathyurus  conicus,  B.  seelyi. 

Additional  notes  on  Asaphus  canalis 

Conrad. 

In  Bull.  Am.  Mus.  Nat.  Hist.,  New  York,  vol. 
2,  No.  2, 1889,  p.  64,  pis.  11, 12. 

Description  of  a new  form  of  fossil, 

Balanoid  Cirripede,  from  the  Marcellus 
shale  of  New  York. 

In  Bull.  Am.  Mus.  Nat.  Hist.,  New  York,  vol. 
2,  No.  2, 1889,  p.  66. 

Protobalanus  n.  g.,  P.  hamiltonensis,  pi.  13, 
fig.  22. 

See  Hall  (James)  and  Whitfield 

(R.P.). 

Wigand  (Georg  von).  Ueber  die  Trilo- 
biten  der  silurischen  Geschiebe  in 
Mecklenburg. 

In  Zeitschr.  Deutsch.  geol.  Ges.,  vol.  40, 1888, 
p.  39,  pis.  6-10. 

Phacops,  Lichas,  L.  (Hoplolichas),  Illcenus, 
Cheirurm,  0.  (Oyrtometopus),  O.  ( Pseudosphce - 
rexochus),  O.  (Nieszkowskia) , Sphcerexochus, 
Amphion,  Cybele,  Encrinurus,  Acidaspis. 

Wiik  (F.  G.)  Om  fossilierna  i Alands 
silur-kalksten  jemfdrda  med  de  i 
Sverige  och  Estland  fdrekommande.  (*) 

In  Bidrag  till  Kannedom  af  Finlands  Natur 
och  Folk,  pt.  35,  Helsingfors,  1881. 


74 


A BIBLIOGRAPHY  OP  PALEOZOIC  CRUSTACEA. 


[BULL.  63. 


Wilckens  (C.  F.)  Sendschreiben,  worm 
wahrscheinlich  dargethan  wird,  dass  die 
Conchilioligisten  eben  keine  Ursache 
mebr  baben,  das  Petrefact,  welcbes 
bisber  unter  der  Benenmmg  eines  Uon- 
chitce  trilobi  ragosi  bekannt  geworden 
ist,  als  einen  Tbeil  ihrer  Wissenscbaft 
anzusehen.  (*) 

In  Stralsundisches  Mag.,  vol.  1, 1768,  p.  267. 

Nachricht  von  seltenen  Versteine- 

rungen,  vornemlicb  des  Thier-Reiches, 
welcbe  bisber  nocb  nicht  genau  genug 
bescbieben  und  erklart  worden.  Mit 
Kupfern,  in  drei  Sendsebreiben  an  seine 
Gonner  und  Freunde.  Berlin  und 
Stralsund,  1769,  pi.  8.  (*) 

Williams  (EL  S.)  On  the  occurrence  of 
Proetus  longicauda  Hall  in  Madison 
County,  Kansas. 

In  Am.  Jour.  Sci.,  3d  series,  vol.  21,  1881,  p. 

156. 

Notice  of  a new  Limuloid  Crustacean 

from  the  Devonian. 

In  Amt  Jour.  Sci.,  3d  series,  vol.  30, 1885,  p.  45, 
3 figs. 

Prestwichia  eriensis  n.  s. 

This  species  was  used  by  A.  S.  Packard 
(Mem.  Nat.  Acad.  Sci.,  vol.  3, 1888,  p.  150)  for  the 
type  of  bis  new  genus,  Protolimulus. 

Notice  of  a new  Limuloid  Crustacean 

from  the  Devonian  formation  of  Erie 
County,  Pennsylvania. 

In  Nature,  vol.  32,  London,  1885,  p.  350. 

Prestwichia  eriensis. 

Winchell  (Alexander).  Descriptions  of 
fossils  from  the  Marshall  and  Huron 
groups  of  Michigan. 

In  Proc.  Acad.  Nat.  Sci.  Phila.,  vol.  14, 1862,  p. 
405. 

Oythere  crassimarginata. 

Description  of  fossils  from  the 

yellow  sandstone  lying  beneath  the 
Burlington  limestone  at  Burlington, 
Iowa. 

In  Proc.  Acad.  Nat.  Sci.  Phila.,  vol.  15,  1863, 

p.  2. 

Phillip8ia  insignis,  P.  meramecensis. 

Notice  of  a small  collection  of  fossils 

from  the  Potsdam  sandstone  of  Wis- 
consin and  Lake  (Superior  sandstone  of 
Michigan. 

In  Am.  Jour.  Sci.,  2d  series,  vol.  37,  1864,  p. 
226. 

Dicellocephalus,  Ptychaspis. 

Description  of  new  species  of  fossils 

from  the  Marshall  group  of  Michigan 


Winchell  (Alexander) — Continued, 
and  its  supposed  equivalent  in  other 
States;  with  notes  on  some  fossils  of 
the  same  age  previously  described. 

In  Proc.  Acad.  Nat.  Sci.  Pbila.,  vol.  17,  1865, 
p.  109.  . 

Phillipsia  rockfordensis , P.  doris  (Hall)  Win- 
chell. 

and  Marcy  (O.)  Enumeration  of 

the  fossils  collected  in  the  Niagara 
limestone  at  Chicago,  111. ; with  de- 
scriptions of  some  new  species. 

In  Mem.  Boston  Soc.  Nat.  Hist.,  vol.  1, 1866,  p. 

81,  pis.  2,  3. 

Lichas,  Addaspis,  Bronteus,  Illcenus. 

Winchell  (N.  H.)  Fossils  from  the  red 
quartzite  at  Pipestone. 

In  13th  Kept.  Geol.  Nat.  Hist.  Survey  Minne- 
sota, 1884,  p.  65,  plate. 

Paradoxides  barberi. 

Woltersdorf  (J.  L.)  Systema  minerale. 
Berlin,  1748,  p.  42. 

The  author  classes  the  Trilobites  with  the 
Mollusca,  calling  them  “Conchites  trilobus.” 

Woodward  (Henry).  On  a nearly  per- 
fect specimen  of  Eurypterus  lanceolatus 
(Salter)  from  the  Upper  Ludlow  rocks 
at  Lesmahagow,  etc. 

In  Geol.  Mag.,  vol.  1,  London,  1864,  p.  107,  pi.  5. 

On  the  Eurypteridcv  and  Xiphosura. 

In  Kept.  34th  Meeting  Brit.  Assoc.  Adv.  Sci.,' 

1864,  Sec.  C;  Geol.  Mag.,  vol.  1,  London,  p.  239. 
Eurypterus , Pterygotus,  Slimonia,  Stylo  nu~ 

rus , Eemiaspis. 

Descriptions  of  some  new  Palaeozoic 

Crustacea. 

In  Geol.  Mag.,  vol.  1,  London,  1864,  p.  196,  pi. 

10,  wood-cuts.  - 

Eurypterus,  Pterygotus,  Stylonurus. 

On  some  Crustacean  teeth  from  the 

Carboniferous  and  Upper  Ludlow  rocks 
of  Scotland. 

In  Geol.  Mag.,  vol.  2,  London,  1865,  p.  401, 
pi.  11. 

Ceratiocaris,  Dithyrocaris. 

On  some  new  species  of  Crustacea 

belonging  to  the  order  Eurypteridce. 

In  Geol.  Mag.,  vol.  2,  London,  1865,  p.  319;  j 
Quart.  Jour.  Geol.  Soc.  Loudon,  vol.  21, 1865,  p.  I 
482,  pi.  IB. 

Stylonurus  powriei  Page,  S.  scoticus  n.  s. 

On  the  discovery  of  a new  genus  of  > 

Cirripedia  in  the  Weulock  limestone,  I 
Dudley. 

In  Quart.  Jour.  Geol.  Soc.  London,  vol.  21, 

1865,  p.  486,  pi.  14;  Geol.  Mag.,  vol.  2,  London, 

1865,  p.  319. 

Turrilcpas  n.  g. 


VOGDEB.] 


LIST  OF  AUTHORS. 


75 


Woodward  (Henry)— Continued. 

On  a new  genus  of  Eurypterida  from 

the  Lower  Ludlow  rocks  of  Leintwar- 
dine,  Shropshire. 

In  Quart.  Jour.  Geol.  Soc.  London,  vol.  21, 
1865,  p.  490,  pi.  14. 

Hemiaspis  n.  g. 

and  Salter  (J.W.)  Chart  of  the 

genera  of  fossil  Crustacea.  See  Salter 
(J.  W.)  and  Woodward  (Henry). 

Shield  bearing  Crustacea,  recent 

and  fossil. 

In  Intellectnral  Observer,  vol.  8,  1865,  p.  321, 
plate. 

Harpes. 

First  report  on  the  structure  and 

classification  of  fossil  Crustacea. 

In  Kept.  35th  Meeting  Brit.  Assoc.  Adv.  Sci., 

1865. 

On  a new  Phyllopodous  Crustacean. 

In  Kept.  35th  Meeting  Brit.  Assoc.  Adv.  Sci., 

1865,  Trans,  of  Sec.,  p.  78. 

Discinocaris  n.  g.,  D.  browniana  Woodward. 
For  description  and  illustration  of  Discino- 
caris, see  Quart.  Jour.  Geol.  Soc.,  vol.  22, 1866. 

On  the  occurrence  of  Ceratiocaris  in 

the  Wenlock  limestone  of  England. 

In  Geol.  Mag.,  vol.  3,  London,  1866,  p.  203, 

pi.  10. 

Note  on  some  fossil  Crustacea  and  a 

Chilognathous  Myriapod  from  the  Coal 
Measures  of  the  west  of  Scotland. 

In  Trans.  Geol.  Soc.  Glasgow,  vol.  2,  1866,  p. 
234,  pi.  3,  wood-cuts. 

On  a new  genus  of  Phyllopodous 

Crustacean  from  the  Moffat  shales, 
Dumfriesshire. 

In  Quart.  Jour.  Geol.  Soc.  London,  vol.  22, 

1866,  p.  503,  pi.  25. 

Discinocaris  n.  g.,  L>.  browniana , Peltocaris 
aptychoides. 

See.  also,  Kept.  35th  Meeting  Brit.  Assoc. 
Adv.  Sci.,  1865,  Trans,  of  Sec.,  p.  78. 

Second  report  on  the  structure  and 

classification  of  the  fossil  Crustacea. 

In  Kept.  36th  Meeting  Brit.  Assoc.  Adv.  Sci., 

1866,  p.  71. 

Eurypterida , Xiphosura. 

On  some  points  in  the  structure  of 

the  Xiphosura,  having  reference  to  their 
' relationship  with  the  Eurypteridw. 

In  Quart.  Jour.  Geol.  Soc.  London,  vol.  23, 

1867,  p.  28,  pis.  1,2. 

Eurypterida:  Pterygotus  Agas.,  Slimonia 
(Page)  Woodward,  Stylonurus  (Page)  Wood- 
ward, Eurypterus  De  Kay  subgenus,  Dolichop. 
terns  Hall,  Adelopthalmus  Jordan,  Bunodes 
Eichw.,  Arthropleura  Jordan,  Hemiaspis 


Woodward  (Henry)— Continued. 

Wood.,  Exapinurus  Nieszk.,  Pseudoniscus 
Nieszk.  Xiphosura:  Belinurus  (Konig)  Baily, 
Prestwichia  n.  g.,  Limulus  Muller. 

A monograph  of  the  British  fossil 

Crustacea  of  the  order  Mesostomata. 

In  Palaeont.  Soc.  London,  pt.  1,  1866 ; pt.  2, 
1868;  pt.3, 1871;  pt.  4, 1872;  pt.  5, 1877,  36  pis. 

Pterygotus,  Slimonia,  Stylonurus,  Eurypterus , 
Hemiaspis,  Belinurus , Neolimuhis,  Prestwichia, 
Limulus,  Cyclus. 

Third  report  on  the  structure  and 

classification  of  the  fossil  Crustacea. 

In  Rept.  37th  Meeting  Brit.  Assoc.  Adv.  Sci., 

1867,  p.  44.  _ „ . 

Eurypterus,  Pterygotus,  Prceatya,  Gomocy • 

poda. 

Recent  and  fossil  Crustacea ; being 

a lecture  delivered  before  the  Geologi- 
cal Association,  December  12,  1867. 

In  Geol.  Mag.,  vol.  5,  London,  1868,  p.  33; 
Rept.  Geol.  Assoc.,  1867;  notice  of  lecture. 

On  a new  Limuloid  Crustacean  ( Neo - 

limulus  falcatus),  from  the  Upper  Silu- 
rian of  Lesmahagow,  Lanarkshire. 

In  Geol.  Mag.,  vol.  5,  London,  1868,  p.  1,  pi.  1. 

On  a newly  discovered  long-eyed 

Calymene  from  the  Wenlock  limestone. 
Dudley. 

In  Geol.  Mag.,  vol.  5,  London,  1868,  p.  489, 
pi.  21. 

Contributions  to  British  fossil  Crus- 
tacea. 

In  Geol.  Mag.,  vol.  5,  London,  1868,  p.  258; 
also  p.  353,  pis.  14, 17. 

Pyrgoma  Crustacea,  Glyphea , and  Pseudogly, 
phea. 

On  some  new  species  of  Crustacea 

from  the  Upper  Silurian  rocks  of  Lan- 
arkshire, etc.  ; and  further  observations 
on  the  structure  of  Pterygotus. 

In  Quart.  Jour.  Geol.  Soc.  London,  vol.  24, 
1868,  p.  289,  pis.  9, 10. 

Eurypterus  ( Pterygotus ) punctatus  Salter, 
Eurypterus  scorpioides  n.  s.,  E.  obesus  n.  s. 
Pterygotus  raniceps  n.  s. 

Fourth  report  on  the  structure  and 

classification  ot  the  fossil  Crustacea. 

In  Rept.  38th  Meeting  Brit.  Assoc.  Adv.  Sci., 

1868,  p.  72,  pi.  2. 

Neolimulus  falcatus  sp.  et  gen.  nov.,  Cyclus 
radialis  Dekon. 

On  the  occurrence  of  Stylonurus  in 

the  “ cornstone  ” of  Herefordshire. 

In  Rept.  39 tb  Meeting  Brit.  Assoc.  Adv.  Sci., 

1869,  Trans,  of  sec.,  p.  103. 

| Note  on  the  palpus  and  other  ap- 

pendages of  an  Asaphus  from  the  Tren- 
ton limestone  in  the  British  Museum. 


[bull.  63. 


76  A BIBLIOGRAPHY  OP  PALEOZOIC  CRUSTACEA. 


Woodward  (Henry) — Continued. 

In  Quart.  Jour.  Geol.  Soc.  London,  vol.  26, 
1870,  p.  486,  wood-cut. 

On  the  remains  of  a giant  Isopod, 

Prcearcturus  gigas,  from  the  Old  Red 
Sandstone  of  Rowlestone  quarry,  Here- 
fordshire. 

In  Trans.  Woolhope  Nat.  Field  Club,  1870, 
p.  266,  3 pis. 

On  Necrogrammarus  salweyi,  lower 

Ludlow,  Leintwardine. 

In  Trans.  Woolhope  Nat.  Field  Club,  1870, 
p.  271. 

On  Eurypterus  brodiei,  from  Perton, 

Hereforshire. 

In  Trans.  Woolhope  Field  Club,  1870,  p.  276, 
2 pis. 

Notes  on  fossil  Crustacea. 

In  Kept.  40th  Meeting  Brit.  Assoc.  Adv.  Sci., 

1870,  Trans,  of  sec.,  p.  91. 

Eurypterus , Cemtioca.ru,  Cyclus,  Dithyro- 
caris. 

Contributions  to  British  fossil  Crus- 
tacea. 

In  Geol.  Mag.,  vol.  7.  London,  1870,  p.  554, 

pi.  22. 

Cyclus. 

On  the  structure  of  Trilobites. 

In  Geol.  Mag.,  vol.  8,  London,  1871,  p.  289, 
pi.  8. 

Asaphus  platycephalus  Stokes. 

On  some  new  Phyllopodous  Crusta- 
ceans from  the  Palaeozoic  rocks. 

In  Geol.  Mag.,  vol.  8,  1871,  p.  104,  pi.  3. 

Ceratiocaris,  Dithyrocaris. 

Extract  published  in  the  Canadian  Natural- 
ist, n.  s.,  vol.  6,  1871,  p.  18. 

Fifth  report  on  the  structure  and 

classification  of  the  fossil  Crustacea, 
etc. 

In  Rept.  41st Meeting  Brit.  Assoc.  Adv.  Sci., 

1871,  p.  53;  also,  Geol.  Mag.,  vol.  8,  London, 
1871,  p.  521. 

On  a new  species  of  Eurypterus  ( E . 

brodiei)  from  Perton,  near  Stoke  Edith, 
Herefordshire. 

In  Quart.  Jour.  Geol.  Soc.  London,  vol.  27, 
1871,  p.  261,  figures. 

On  a new  fossil  Crustacean,  from  the 

Devonian  of  Canada. 

In  Canadian  Naturalist,  n.  s.,  vol.  6,  1871, 

p.  18. 

Dithyrocaris. 

Note  on  some  British  Palaeozoic 

Crustacea  belonging  to  the  order  Me- 
sostomata. 

In  Geol.  Mag.,  vol.  9,  London,  1872,  p.  433, 

pi.  10. 


Woodward  (Henry) — Continued. 

Hemiaspis , Pseudoniscus , Exapinurus , Buno - 
des,  Bellinurus,  Prestwichia. 

Further  remarks  on  the  relationship 

of  the  Xiphosura  to  the  Eurypteridae, 
and  to  the  Trilobita,  etc. 

In  Quart.  Jour.  Geol.  Soc.  London,  vol.  28, 
1872,  p.  46,  figures;  also,  Annals  Mag.  Nat. 
Hist.  London,  4th  series,  vol.  9,  London,  1872, 
p.  406. 

Sixth  report  on  the  structure  and 

classification  of  the  fossil  Crustacea, 
etc. 

In  Rept.  42d  Meeting  Brit.  Assoc.  Adv.  Sci., 
1872,  p.  321;  also,  Geol.  Mag.,  vol.  9,  London, 

1872,  p.  563. 

Life  forms  of  the  past  and  present. 

In  Popular  Sci.  Review,  vol.  11,  London, 

1873,  p.  391,  pis.  90,91. 

Pterygotus,  Slimonia,  Stylonurus , Eurypterus, 
Hemiaspis,  Prestwichia,  Bellinurus,  Neolimu- 
lus,  Dithyrocaris,  Trinucleus  ornatus,  Sao  hir . j 
suta. 

On  a new  Trilobite  from  the  Cape  of 

Good  Hope. 

In  Quart.  Jour.  Geol.  Soc.  London,  vol.  29, 
1873,  p.  32,  pi.  2. 

Encrinurus  crista-galli. 

Seventh  report  of  the  committee  ap- 
pointed for  the  purpose  of  continuing 
researches  in  fossil  Crustacea,  consisN 
ing  of  Prof.  P.  Martin  Duncan,  Henry 
Woodward,  and  Robert  Etheridge. 

In  Rept.  43d  Meeting  Brit.  Assoc.  Adv.  Sci., 'a 
1873,  p.  304 ; also,  Geol.  Mag. , vol.  10,  London, 
1873,  p.  520. 

Olenus  utahensis  n.  s. 

and  Etheridge,  jr.  (Robert).  On 

some  specimens  of  Dithyrocaris , from  the 
Carboniferous  limestone  series,  East ' 
Kilbride,  and  the  Old  Red  Sandstone  of 
Lanarkshire. 

In  Geol.  Mag.,  vol.  10,  London,  1873,  p.  482, 
pi.  16. 

On  some  specimens  of  Dithyro- 
caris, from  the  Carboniferous  limestone  j 
series,  East  Kilbride,  and  from  the  old  j 
red  sandstone  of  Lanarkshire. 

In  Rept.  Brit.  Asso.,  vol.  43,  1873,  Trans,  of  i 
sec.,  p.  92. 

Eighth  report  on  fossil  Crustacea.  ' 

In  Rept.  45th  Meeting  Brit.  Assoc.  Adv.  Sci.,  'J 
1875 ; also,  Geol.  Mag.,  new  series,  decade  2,  vol.  j 
2,  1875,  p.  620. 

Two  lectures  on  receut  and  fossil 

Crustacea  delivered  at  the  Royal  Insti- 
tution, on  April  29  and  May  6,  1876. 

In  Proc.  Royal  Inst.  Gr.  Brit.,  1876;  Times,  I 
Morning  Post,  Illustrated  News,  1876. 


POGDES.] 


LIST  OF  AUTHORS, 


77 


Woodward  (Henry)— Continued. 

A catalogue  of  British  fossil  Crus- 
tacea, with  their  synonyms  and  the 
range  in  time  of  each  genus  and  order. 
Published  by  order  of  the  trustees  of 
the  British  Museum  1877. 

A review  of  the  book  was  published  in  the 
Geol.  Mag.,  decade  2,  vol.  4,  J877. 

Note  on  the  genus  Anthrapalcemon 

( Pdlceocarabus ) of  Salter  from  the  Coal 
Measures. 

In  Geol.  Mag.,  decade  2,  vol.  4, 1877,  p.  55. 

Article  “ Crustacea.” 

In  Ency.  Britannica,  vol.  6, 1877,  86  wood-cuts. 

Asaphus,  Trinucleus,  Sao,  Aridaspis,  Para- 
doxides. 

Discovery  of  the  remains  of  a fossil 

crab  (Decapoda-Br achy ura)  in  the  Coal 
Measures  of  the  environs  of  Mons, 
Belgium. 

In  Geol.  Mag.,  decade  2,  vol.  5,  London,  1878, 
p.  433,  pi.  11. 

Brachypyge  carbonis  Wood. 

Note  on  Palaeozoic  Crustacea. 

In  Geol.  Mag.,  decade  2,  vol.  6,  1879,  p.  196, 

! pl-5. 

Eurypterus  scouleri. 

\ A new  genus  of  Trilobites  Onycopyge 

liver8idgei,  from  South  Wales. 

In  Geol.  Mag.,  decade  2,  vol.  7,  1880,  p.  97, 

figure. 

Note  on  a new  English  Homalonotus 

from  the  Devonian,  Torquay,  South 
Devon. 

In  GeoLMag.,  decade'2,  vol.  8,  London,  1881, 
p.  489,  pi.  13. 

Homalonotus  champernownei 

Contributions  to  the  study  of  fossil 

Crustacea. 

In  GeoL  Mag.,  decade  2,  vol.  8,  London,  1881, 
p.  529,  pi.  14. 

Eryon  perroni,  Palceocaru  burnettii,  figure, 
p.  533,  pi.  14,  tig.  3. 

Additional  note  on  Homalonotus  from 

the  Devonian. 

In  Geol.  Mag.,  decade  2,  vol.  9,  London,  1882, 

p.  157,  pi.  4. 

Homalonotus  goniopygoeus,  H.  champernow- 

nei. 

I Note  on  Ellipsocaris  deivalquei,  a new 

Phyllopod  from  the  Upper  Devonian  of 
Belgium. 

In  Geol.  Mag.,  decade  2,  vol.  9,  London,  1882, 
p.  444,  figures. 

On  a series  of  Phyllopod  Crustacean 

shields  from  the  Upper  Devonian  of  the 


Woodward  (Henry)— Continued. 

Eilel;  and  on  one  from  the  Wenlock 
shales  of  Wales. 

In  Geol.  Mag.,  new  series,  decade  2,  vol.  9, 
London,  1882,  p.  385,  pi.  9. 

Gardiocaris  n.  g.,  Pholadocaris  n.  g.,  Apty- 
chopis. 

Synopsis  of  the  genera  and  species 

of  Carboniferous  limestone  Trilobites. 

In  Geol.  Mag. . new  series,  decade  2,  vol.  10, 
London,  1883,  pp.  445, 481, 534,  pis.  11-13. 

Phillip8ia,  Griffithides,  Brachymetopus. 

Edition  by  author  3 pis.  and  26  pp. 

Synonyms  of  Phillipsia  gemmulifera. 

In  Geol.  Mag.,  decade  3,  vol.  1,  London,  1884 

p.  22. 

Monograph  of  the  British  Carbonif- 
erous Trilobites. 

In  Palaeont.  Soc.  London,  pt.  1, 1883,  pp.  1-38, 
pis.  1-6.  Phillipsia , Griffithides.  Pt.  2 (conclu- 
sion), 1884,  pp.  39-83,  pis.  7-10. 

Proetus,  Phillipsia , Brachymetopus , Griffi- 
thides,  Dalmanites? . 

On  the  structure  of  Trilobites. 

In  Geol.  Mag.,  decade  3,  vol.  1,  London,  1884, 
p.  78. 

Asaphus. 

Appendages  of  Trilobites. 

In  Geol.  Mag.,  decade  3,  vol.  1,  London,  1884, 

p. 162. 

Asaphus  megistos , 2 figs. ; Oalymene. 

Note  on  the  remains  of  Trilobites 

from  South  Australia. 

In  Geol.  Mag.,  decade  3,  vol.  1,  London,  1884, 
p. 342. 

Conocephalites , Dolichometopus . 

Synopsis  of  the  genera  and  species 

of  Carboniferous  limestone  Trilobites. 

In  Geol.  Mag.,  decade  3,  vol.  1,  London,  1884, 
p.  484,  pi.  16. 

Phillipsia  laticaudata,  P.  scabra,  P.  carinata , 
Griffithides  brevispinus,  G.  glaber,  G.  ? carring- 
tonensis. 

On  the  discovery  of  Trilobites  in  the 

Culm  shales  of  southeast  Devonshire. 

In  Geol.  Mag.,  decade  3,  vol.  1, 1884,  p.  534. 

Phillipsia  lei,  P.  minor,  P.  cliffordi,  P.  articu- 
losa. 

and  Jones  (T.  Rupert).  Notes  on 

the  phyllodiform  Crustacea,  referable 
to  the  genus  Edinocaris,  from  the  Pa- 
laeozoic rocks. 

In  Geol.  Mag.,  decade  3,  vol.  1,  London,  1884, 
p.  393,  pi.  13. 

Ceratiocari8. 

On  some  Palaeozoic  Phyllopod  shields 

and  on  Nebalia  and  its  allies. 

In  Geol.  Mag.,  decade  3,  vol.  2,  London,  1885, 
p.  345,  pi.  9. 


78 


A BIBLIOGRAPHY  OF  PALEOZOIC  CRUSTACEA. 


[BULL.  63. 


Woodward  (Henry) — Continued. 

Notice  of  a new  limuloid  Crustacean 

from  the  Devonian,  by  H.  S.  Williams. 

In  Geol.  Mag.,  decade  3,  vol.  2,  London,  1886, 
p.  427. 

On  the  discovery  of  Trilobites  in  the 

Upper  Green  (Cambrian)  slates  of  the 
Penrhyn  quarries,  Bethesda,  near  Ban- 
gor, North  Wales. 

In  Quart.  Jour.  Geol.  Soc.  London,  vol.  44, 
1888,  p.  74,  pi.  6. 

Oonocoryphe  viola  Wood. 

On  the  discovery  of  Trilobites  in  the 

Upper  Green  (Cambrian)  slates,  etc., 
North  Wales. 

In  Rept.  57 tli  Meeting  Brit.  Assoc.  Adv.  Sci., 
1887,  p.  696. 

Conocoryphe  viola. 

On  a new  species  of  Eurypterus  from 

the  Lower  Carboniferous  shale,  Esk- 
dale,  Scotland. 

In  Rept.  57th  Meeting  Brit.  Assoc.  Adv.  Sci., 
1887,  p.  696. 

See  Jones  (T.  Rupert)  and  Wood- 
ward (H$nry). 

See  Etheridge  (Robert)  and  Wood- 
ward (Henry). 

Worthen  (A.  H.)  Description  of  two 
new  species  of  Crustacea,  fifty-one  spe- 
cies of  mollusca,  and  three  species  of 
Crinoids  from  the  Carboniferous  forma- 
tion of  Illinois  and  adjacent  States. 

In  Bull.  No.  2 State  Mus.  Nat.  Hist.  Hlinois, 
1884. 

Colpocaris  Chester ensis,  Solenocaris  St.Ludo- 
vici. 

See  also  Meek  (F.  B.)  and  Worthen  (A.  H.) 

Young  (J.)  Descriptive  notes  of  several 
new  and  rare  forms  of  Entomostraca. 

In  Trans.  Geol.  Soc.  Glasgow,  vol.  5,  pt.  2, 
1877. 

On  the  Silurian  strata  of  Pen- 

whapple  Glen,  near  Girvan. 

In  Proc.  Nat.  Hist.  Soc.  Glasgow,  vol.  1,  pt.  2, 
1868,  p.  171;  also  in  Proc.  Royal  Phys.  Soc.  Edin- 
burgh, vol.  4, 1878. 

Solenocaris  n.  g.  (not  Solenocaris  Meek.). 

Zenker  (J.  C.)  Beitrage  zur  Naturge- 
schichte  der  Urwelt.  Organische  Reste 


Zenker  (J.  C.) — Continued. 

(Petrefacten)  rus  der  Altenburger 
Braunkohlen-Formation,  dem  Blanken- 
burger  Quadersandstein,  jenaischen 
bunten  Sandstein  und  bohmischen 
Uebergangsgebirge,  mit  6 illuminirten 
Kupfertafeln.  Jena,  1833. 

Olenus  longicaudatus,  O.  pyramidalis,  O. 
latus,  Otarion  n.  g.,  O.  diffractum,  O.  ? squar- 
rosum,  Oonocephalus  n.  g.,  C.  costatus,  Ellipso- 
cephalus  n.  g.,  E.  ambiguus. 

The  genus  Otarion  was  made  up  from  the 
head  of  Oyphaspis  burmeisteri  Barr.,  connected 
with  the  pygidium  of  Gromits  beamonti  Barr. 
The  second  species,  described  as  Otarion  f 
squarrosum , is  referred  by  Joachim  Barrande 
to  Cheirurus  quenstadi. 

J.  C.  Zenker  uses  two  generic  names  for  his 
new  genus  Oonocephalus,  the  first  on  p.  48  in 
describing  the  genus  and  the  second  in  his  de- 
scription of  plate  5,  where  he  calls  it  Trigono- 
cephalus. 

Both  these  generic  terms  had  been  used  in 
natural  history  for  other  genera,  the  first  by 
Thurnburg  in  1812  for  a genus  of  the  Orthop- 
tera,  and  the  second  by  Oppel  in  1811  for  the 
Reptiles. 

The  typical  species  described  as  Oonocephalus 
costatus  on  p.  49,  and  also  in  the  explanation  of 
pi.  5,  figs.  G-K,  p.  51,  and  as  Trigonocephalus 
costatus  in  the  description  of  pi.  5,  given  on  p. 
51,  has  been  referred  by  Joachim  Barrande  to 
an  amended  genus,  Conocephalites  (Zenker) 
Barr.,  and  the  species  to  the  older  name  of 
sulzeri.  The  other  new  genus,  Ellipsocephalus, 
has  been  used  by  all  subsequent  authors. 

Zeno  (Franz).  Yon  Seeversteinerungen 
und  Fossilien,  welche  bei  Prag  zu  finden 
Sind. 

In  Nene  phys.  Belustigungen,  etc.,  vol.  1, 
1770,  p.  65.  Continued  same  vol.,  p.  362,  pi.  1, 
fig.  1. 

Under  the  names  of  Cacada  or  K'dfermuschcl 
Franz  Zeno  describes  the  pygidium  of  Dal- 
manites  hausmanni  and  the  head  of  Phacops 
latifrons. 

Zittel  (Karl  A.)  Handbuch  der  Palseon- 
tologie.  Vol.  2.  Miinchen  und  Leip- 
zig, 1881-’85,  p.  525. 

! Zippe  (F.  X.)  See  Sternberg  (Kasper 
| Graf  yon). 


PART  II. 


CATALOGUE  OF  TRILOB1TES, 


PART  II 


A SYSTEMATIC  CATALOGUE  OF  AMERICAN  PALEOZOIC  CRUSTACEA, 

TRILOBITA. 


First  series , with  grooved  pleurae. 


Family. 

Genera. 

Reference. 

Harpedidm 

Harpes  Goldfuss,  1839  

Nova  Acta  Physico-Med.,  vol.  19,  p.  358.  Type, 
Harpes  macroceplialus  Gold.,  Harpes  ungula 
Sternb.  Barrande,  Syst.  Sil.  Boheme,  vol.  1;  p. 
347,  pis.  3-9. 

Remopleuridfe . 

Remopleurides  Portlock,  1843 

Geol.  Rept.  Londonderry,  etc.,  p.254.  Type,  Be- 
mopleurides  colbii  Portlock. 

Paradoxidae 

Paradoxides  Brongniart,  1822 

Hist.  Crust.  Foss.,  p.  30.  Type,  Paradoxides  tes- 
sini  Brong. 

Anopolenus  Salter,  1864  

Geol.  Soc.  London  Jour.,  vol.  20,  p.  236.  Type, 

Anopolenus  henrici  Salter. 

Bathynotus  Hall,  1860  

Thirteenth  Rept.  New  York  'State  Cab.  Nat. 
Hist.,  p.  117.  Type,  Bathynotus  holopyga  Hall. 

Dicellocephalus  Owen,  1852 

Rept.  Geol.  Survey  Wisconsin,  Iowa,  and  Minne- 
sota, p.  573.  Type,  Dikelocephalus  minnesotensis 

Owen. 

Mesonacis  Walcott,  1884 

Am.  Jour.  Sci.,  3d  series, vol.  29,  p.  329.  Type,  Ole- 
nus vermontana  Hall. 

Dolichometopus  Angelin,  1854 

Palseont.  Scand.,  p.  72.  Type,  Dolichometopu 
svecicus ; Ang.  Palseont.  Scand.,  p.  73,  pi.  37, 

fig.  9. 

Hydrocephalus  Barrande,  1846 

Notice  Pr61im.  Syst.  Sil.  Bohfime,  p.  18.  Type, 
Hydrocephalus  carens  Barr.  Notice  Pr61im. 
Syst.  Sil.  Boheme,  p.  19. 

Olenellns  Hall,  1861 

Fifteenth  Rept.  New  York  State  Cab.  Nat.  Hist., 
p.  114.  Type,  Olenellus  thompsoni  Hall.  Twelfth 
Rept.  Now  York  State  Cab.  Nat.  Hist.,  p.  59, 
figure. 

Olenus  Dalman,  1826 

Palaead.,  p.  56.  Type,  Olenus  gibbosus  Wahlen- 
bnrg. 

Zacanthoides  Walcott,  1887 

Am.  Jour.  Sci.,  3d  scries,  vol.  36,  p.  165.  Typo, 
Olenoides  spinosus  Walcott. 

Parabolina  Salter,  1849 

Mem.  Geol.  Survey  United  Kingdom,  decade  2. 
Type,  Olenus  spimdosa  Wahl. 

I’eltura  Milno-Edwards,  1840  

Hist.  Nat.  Crust.,  vol.  3,  p.  344.  Typo,  Olemcs 

scarabcenides  Wahl. 

Cyclognathus  Linnarsson,  1875  . . . 

Geol.  Foreuingens  Stockholm  Forhandl.,  vol.  2, 
No.  12,  p.  500.  Type,  Cyclognathus  mioropygus 
Linnarsson. 

81 

Bull.  63 6 


82  A BIBLIOGRAPHY  OF  PALEOZOIC  CRUSTACEA.  [bull.  63. 

First  series, grooved  pleurae— Continued. 


Family. 

Genera. 

Reference. 

Paradoxides  . . - 

Triarthrus  Green,  1832 

Mon.  Trilobites  North  America,  p.  87.  Type, 
Triarthrus  beckii  Green. 

Leptoplastus  Angelin,  1854 

Subgenera: 

Pakeont.  Scand.,  p.  46.  Type,  Leptoplastus  steno- 
tus  Angelin. 

1.  Sphserophtkalmus  Angelin, 

Palaeont.  Scand.,  p.  49.  Type,  Sphcerophthalmus 

1854. 

flagellifer  Aug. 

2.  Ctenopyge  Linnarsson,  1880. 

Geol.  Fdreningens  Stockholm  Forhandl.,  vol.  5,  p. 
145.  Type,  Olenus  ( Sphcerophthalmus ) pecten 

. 

Salter. 

Bceckia  Brogger,  1882 

Die  silurischeD  Etagen  2 und  3,  p.  122.  Type, 

Bceckia  hirsuta  Brogger. 

Ceratopyge  Corda,  1847 

Prodr.,  p.  161.  Type,  Olenus  for ficular  Sara. 

Bohemillidas . . . 

Bohemilla  Barrande,  1872  

Svst.  Sil.  Bolifime,  vol.  1,  Snppl.,  p.  137.  Type, 

Bohemilla  stujrenda  Barr. 

Conocoryphidte 

Atops  Emmons,  1844 

Taconic  System,  p.  20.  Type,  Atops  trilineatus 
Emmons. 

Conocorvphe  Corda,  1847  

Prodr.,  p.  23.  Type,  Trilobite  sulzeri  Schlutt. 

Ptychoparia  Corda,  1847  

Prodr.,  p.  26.  Type,  Conocephalus  striatus. 

Ctenocephalus  Corda,  1847 

Prodr.,  p.  26.  Type,  Ctenocephalus  barrandi 
Corda. 

Solenopleura  Angelin,  1854  

Paheont.  Scand.,  p.  26.  Type,  Solenopleura  holo- 
metopa  Ang. 

Liostracus  Angelin,  1854 

Palaeont.  Scand.,  p.  27.  Type,  Liostracus  aculea- 
tus  Angelin. 

Aneuacanthus  Angelin,  1854 

Palteont.  Scand.,  p.  5.  Type,  Aneuacanthus  acu- 
tangulus  A ng. 

Anomocare  Angelin,  1854 

Palaeont.  Scand.,  p.  24.  Type,  Anomocare  aculea- 
tus  Angelin. 

Angelina  Salter,  1847  

Mem.  Geol.  Survey  United  Kingdom,  decade  xi. 
Type  Angelina  sedgwicki  Salter. 

Agraulos  Corda,  1847  

Prodr.,  p.  26.  Agraulus  certicephalus  Bair. 

Dorypyge  Dames,  1884 

China  (Richthofen),  vol.  4,  p.  23. 

Bathyurus  Billings,  1859 

Canadian  Naturalist,  vol.  4.  p.  364.  Type,  Asaphus 
extans  Hall. 

Bathyurella  Billings,  1865  

Pal.  Foss.,  vol.  1,  p.  262.  B.  marginatus,  B.  niti 
dus,  B.  expansus  Billings. 

Chariocephalus  Hall,  1863  

Sixteenth  Rept.  New  York  State  Cab.  Nat.  Hist., 
p.  175.  Type,  Chariocephalus  whitfieldi  Hall. 

Corynexochus  Angelin,  1854 

Paheont.  Scand.,  p.  59.  Type,  Corynexochus  spinu- 

Ellipsocepbalus  Zenker,  1833 

losa  Ang. 

Beitrage  Nat.  Urwelt,  p.  31.  Type,  Ellipsoce- 

phalus  ambiguus  Zonker^Ellipsocephahis  hoffi 
Schlott. 

Ptycbaspis  Hall,  1863 

Sixteenth  Rept.  New  York  State  Cab.  Nat.  Hist., 
p.  170.  Type,  Bikelocephalus  minisccensis  Qwen. 

Sao  Barrande,  1846 

Notice  Prdlim.  Syst.  Sil.  Bohdmo,  p.  13.  Type. 
Sao  hirsuta  Barr. 

VODGES.] 


CATALOGUE  OF  TRILOBITES. 


83 


First  series,  with  grooved  pleurae — Continued. 


Family. 

Genera. 

Reference. 

Mem.  Soc.  Geol.  France,  vol.  1,  p.  355.  Type, 
Proetus  cuvieri  Steininger. 

Declienella  Kayser,  1880 

Zeitschr.  Deutscli.  geol.  Gesell.,  Berlin,  vol.  32,  p. 
703.  Type,  Dechenella  verneuili  Barr. 

Prionopeltis  Corda,  1847  ( Phceton 

Prodr.,  p.  121.  Type,  Prionopeltes  polydorus 

Barr.,  Phcet7wnid.es  Angelin), 

Corda. 

Bracliymetopus  McCoy,  1847  

Annals  Mag.  Nat.  Hist.,  1st  series,  London,  vol. 
20,  p.  229.  Type,  Phillipsia  maccoyi  Portlock. 

Cyphaspis  Burmeister,  1843 

Org.  Trilobiten  (Bay  Soc.  Ed.,  p.  98).  Pliacops 
certophthalma  Gold. 

Aretliusina  Barrande,  1852 

Syst.  Sil.  Boheme,  vol.  1,  p.  494.  Arethusina  ko- 
nincki  Barr. 

Harpides  Beyrich,  1846  

TJntersuch.  Trilobiten,  p.  34.  Type,  Harpides 
hospes  Beyrich. 

Cannon  Barrande,  1872  

Syst.  Sil.  Boheme,  vol.  1,  suppl.,  p.  19.  Type,  Gar- 
mon multilus  Barr. 

Cyplioniscus  Salter,  1852 

Kept.  22d  Meeting  Brit.  Assoc.  Adv.  Sci.,  Trans. 
Sec.,  p.  95.  Type,  Cyphoniscus  socialis  Salter. 

Phillipsidae .... 

Pliillipsinella  Novak,  1885  

Sitzungshe.  rbokm.  Gesell.  Wiss.,  1885.  Author’s 
edition,  p.  4.  Type,  Phillipsinella  parabola 
Barr. 

Phillipsia  Portlock,  1843 

Geol.  Kept.  Londonderry,  etc.,  p.  305.  Type, 
Phillipsia  kelli  Portlock =Asaphus  gemmulifera 
Phillips. 

Griffithides  Portlock,  1843 

Geol.  Kept.  Londonderry,  etc.,  p.  310.  Type, 
Griffithides  longiceps  Portlock. 

Dalmanitidas  .. 

Pliacops  Emmrich,  1839 

De  Trilob.,  etc.,  p.  18.  Type,  Phacops  latifions 
Bronn. 

Dalmanites  Emmrich,  1844 

Zur  Nat.  Trilobiten,  etc.,  p.  15.  Barrande’s  Syst. 
Sil.  BohSme,  vol.  suppl.,  p.  27.  Type,  Dalmani- 
tes caudata  Briinnich. 

Coronnra  Hall  & Clarke,  1888 

Pal.  New  York,  vol.  7,  p.  xxxii.  Type,  Coronnra 
aspectens  Conrad. 

Cryph®us  Green,  1837  

Am.  Jour.  Sci.,  1st  series,  vol.  32,  p.  343.  Type, 
Cryphoeus  boothi  Green. 

Chasmops  McCoy,  1849 

Annals  Nat.  Hist.,  2d  series,  vol.  4 ; also  Contrib. 
to  Pal®ont.,  p.  143.  Type,  Calymene  odini 
Eichwald. 

Calymenid® . . . 

Calymeno  Brongniart,  1822 

Crust.  Foss.,  p.  11.  Type,  Calymene  tuberculata 
Briinnich. 

Homalonotus  Koenig,  1825 

leones  Foss.  Sectilos,  p.  7.  Typo,  Homalonotus 

knighli  Koenig. 

Bavarilla  Barrande,  1868 

Fauue  Sil.  des  environs  de  Hof  on  Bavidre,  p.  75. 
Typo,  Bavarilla  ho/ensis  Barr. 

Licliasid® 

Lichas  Dalman,  1826 

Palaiad.,  p.  53.  Type,  Lichas  laciniatus  WaJjl. 

84 


A BIBLIOGRAPHY  OF  PALEOZOIC  CRUSTACEA. 


[BULL.  63. 


First  series , with  grooved  pleurae — Continued. 


Family. 

Genera. 

Reference. 

Trinucleid®  . . . 

Trinucleus  Lhlwyd,  1698  (Crypto- 
lithus  Green,  1832). 

Ampyx  Dalman,  1826. 

Murchison’s  Silurian  Syst.,  1839,  p.  659.  Type, 
Trinucleus  fimbriatus. 

Pal* ad.,  p.  53.  Type,  Ampyx  nasuta  Dalman. 
Neues  Jahrb.  fur  Mineral.,  1847,  pt.  4,  p.  391 ; Syst. 
Sil.  Boheme,  vol.  1,  p.  540.  Type,  Dionidce  for- 
mosa  Barr. 

Mem.  Geol.  Survey  United  Kingdom,  decade  xi, 
pi.  7,  p.  1.  Type,  Salteria  primceva  Thomson. 

! Pal.  Foss.,  vol.  1,  p.  93.  Type,  Endyminia  meeki 
1 Billings. 

Subgenera : 

1.  Saltcria  Thomson,  1864 

2.  Endymima  Billings,  1862... 

Syst.  Sil.  BohOme,  vol.  1,  p.  663.  Typo,  AEglina 
rediviva  Barr. 

IllaBnurid*  — 

Sixteenth  Kept.  New  York  State  Cab.  Nat.  Hist., 
p.  176.  Type,  lllcenurus  quxdratus  Hall.  , 

Asaphid® 

Asaphus  Brongniart,  1822  

Crust.  Foss.,  p.  17.  Type,  Asaphus  expansus 
Wahl. 

Palseont.  Scand.,  p.  51.  Type,  Ptychopyge  appa- 
nata  Ang. 

Mon.  Brit.  Trilobites,  p.  167.  Type,  Asaphus  recti- 
frons  Portlock  and  Asaphus  Icevigatus  Angelin. 

Palaeont.  Scand. , p.  15.  Type,  Megalaspis  gigas 
Angelin. 

Crust.  Foss.,  p.  26.  Type,  Asaphus  buehi  Brong. 

Annals  Nat.  Hist.,  2d  series,  vol.  4,  p.  409.  Type, 
Barrandia  cordai  McCoy. 

Palaeont.  Scand.,  p.  13.  Type,  Asaphus  frontalis 
Dalman. 

Quart.  Jour.  Geol.  Soc.  London,  vol.  33,  p.  663. 
Type,  Asaphellus  homfrayi  Salter. 

Palsead.,  p.  49.  Type,  Xileus  armadillo  Dalman. 

Brachyaspis  Salter,  1866 

Megalaspis  Angelin,  1852 

Ogygia  Brongniart,  1822  

Barrandia  McCoy,  1849  

Niobe  Angelin,  1852  

Asaphellus  Callaway,  1877 

Nilens  "Dalman,  1826  

Second  series,  with  plane  pleurae. 

Stvginidse 

St, yginia  Salter  1853 

Kept.  22d  Meeting  Brit.  Assoc.  Adv.  Sci.,  p.  59. 
Type,  Styginia  latifrons  Portlock. 

Illsenidse 

Illaenus  Dalman,  1826 

Palsead.,  p.  51.  Type,  Illcenus  crassicauda  Wahl. ; 
Nova  Acta  Reg.  Soc.  Sci.  Upsal.,  vol.  8,  p.  27,  pi. 
2^  figs.  3,  5,6.  (Not.  pi.  7,  figs.  5,  6 = Illcenus 
esmarki.) 

Organization  Trilobites,  p.  105  (Ray  Soc.  Ed. 

1846).  Type,  Dysplanus  centrotus  Dalm. 

Sil.  Syst , p.  656.  Type,  Bumastus  barriensis 
Murch. 

M6m.  Acad.  Sci.  Sr.-Petersbourg,  7th  series,  vol.  6, 
No.  2,  p.  31.  Type,  Panderia  triquetra  Volb. 

Dysplanus  Burmeister,  1843 

Bumastus  Murchison,  1839 

Panderia  Yolborth,  1863  

V0GDE6.  ] 


CATALOGUE  OF  TRILOBITES. 


85 


Third  series,  with  ridged  pleurae  ( pleure  a bourrelet,  Barrande). 


Family. 

Genera. 

Reference. 

Acidaspidae  — 

Acidaspis  Muichison,  1839  ( Odon - 
topleura  Emmrich,  1839). 

Silurian  System,  p.  558.  Type,  Acidaspis  brightii 
Murch. 

Ceraurid® 

Ceraurus  Green,  1832  ( Oheirurus 
Beyrich,  1845). 

Spk^rexochus  Beyrich,  1845 

Mon.  Trilobites  N.  A.,  p.  83.  Type,  Ceraurus 
pleurexanthemus  Green. 

TTeber  einige  bohm.  Trilobiten,  p.  19.  Type,  Sphee- 
rexochus  mirus  Beyrich. 

Syst.  Sil.  BohOrne,  vol.  1,  suppl.,  p.  96.  Type,  Areia 
bohemica  Barr. 

Syst.  Sil.  Boheme,  vol.  1,  p.  814.  Type,  Deiphon 
forbesi  Barr. 

Prodr.,  p.  128.  Type,  Placoparia  zippi  Boeck. 

Syst.  Sil.  Boheme,  vol.  1,  p.  810.  Type,  Stauro- 
cephalus murchisoni  Barr. 

Geol.  Mag.,  decade  2,  vol.  7,  p.  97.  Type,  Onyco- 
pyge  liver sidgei  Woodward. 

Staurocephalus  Barrande,  1852 

Ony copy ge  Woodward,  1880  

Amphionid®.  . 

Amphion  Pander,  1850 

Beitrage  Geog.  Russischen  Reiches,  p.  439.  Type, 
Amphion  fischeri  Eichwald. 

Syst.  Sil.  Boheme,  vol.  1,  p.  821.  Type,  Cromus  in- 
tercostatus Barr. 

Cronins  Barrande,  1852 

Encrinurid®... 

Encrinurus  Emmrich,  1844  (Cryp- 
tonymus  Eichwald). 

Cybele  Eoven,  1845  

Zur  Nat.  Trilobiten,  p.  16.  Type,  Trilobus  punc- 
tatus Briinnich. 

Sven  ska  Akad.  Fbrhandl.,  1845,  p.  110.  Type, 
Calymene  bellatula  Dalman. 

Prodr.,  p.  119.  Type,  Dindymene  frederico-au- 
gusti  Corda. 

Dindymene  Corda,  1847  

Brontid® 

BronteuS  Goldfuss,  1843 

Beitrage  Petrefact.,  Nova  Acta  Physico-Med., 
vol.  19,  p.  360.  Type,  Brontes  flabellifer  Gold. 

Fourth  series. 

Agnostid® 

Agnostus  Brongniart,  1822 

Hist.  Crust.  Foss.,  p.  38.  Type,  Agnostus  pisi - 

formis. 

Shumardia  Billing3,  1862 Pal.  Foss.,  vol.  1,  p.  92.  Type,  Shumardia  granu- 

losa Billings. 

Microdiscus  Emmons,  1856 Am.  Geology,  vol.  1,  pt.  2,  p.  116.  As  defined  by 

. Chas.  D.  Walcott,  1886.  Type,  M.  punctatus 

and  M.  speciosus. 


A CATALOGUE  OF  NORTH  AMERICAN  SPECIES  OF  TRILOBITES, 


{Current  names  are  printed  in  bold  face  type;  synonyms  in  Italic .] 

Acantlioloma  Conrad,  1840;  3d  Annual  Rept.  Pal.  Dept.  New  York  Geol.  Survey, 
p.  205.  (See  Acidaspis.) 

spinosa  Conrad.  (See  Acidaspis  tuberculatus.) 

Acidaspis  Murchison,  Silurian  System,  1839,  p.  658. 

Type,  Acidaspis  brightii  Murch.,  Sil.  Syst.,  p.  658,  pi.  14,  figs.  10, 15. 

Syn.,  Cer atocephala  Warder,  1838;  Am.  Jour.  Sci.,  1st  series,  vol.  34,  p.  377. 
Odontopleura  Emmrich,  1839;  De  Tril.,  p.  53. 

Arges  Goldfuss  (iu  part),  Neues  Jahrbuch  fur  Miueral.,  1843,  pp.  544,556. 
Polyeris  Rouault,  1846;  Bull.  Soc.  G6ol.  France,  vol.  4,  p.  320. 

Selenopeltis  Corda,  1847  ; Prodr.,  p.  34. 

Trapelocera  Corda,  1847 ; Prodr.,  p.  158. 

Discranurus  Conrad,  1841 ; 5tli  Ann.  Rept.  Pal.  Dept.  New  York  Geol. 
Survey,  p.  48. 

anchoralis  Miller,  1875;  Cincinnati  Quart.  Jour.  Sci.,  vol.  2,  p.  349,  figs.  2-4. 

Hudson. 

armatn8.  (See  Acidaspis  eriops.) 

callicera  Hall,  1888 ; Pal.  New  York,  vol.  7,  pp.  69, 224,  pi.  16  b,  figs.  1-3. 

Upper  Heidelberg. 

[ Ceratocephala ] ceralepta  Anthony,  1838;  Am.  Jour.  Sci.,  1st  series,  vol.  34,  p. 

379,  figs.  1, 2 Hudson. 

ceralepta  Meek,  1873;  Pal.  Ohio,  vol.  1,  p.  169,  pi.  14,  figs.  8-9. 

ceralepta  Miller,  1874;  Cincinnati  Quart.  Jour.  Sci.,  vol.  1,  p.  130. 

cincinnatiensis  Meek,  1873 ; Pal.  Ohio,  vol.  1,  p.  167,  pi.  14,  fig.  3.  Hudson. 

cincinnatiensis  Miller,  1874 ; Cincinnati  Quart.  Jour.  Sci.,  vol.  1,  p.  130. 

[ Ceraurus]  crosotus  Locke,  1842;  Am.  Jour.  Sci.,  1st  series,  vol.  44,  p.  347,  fig. 

Hudson. 

crosotus  James,  1871 ; Catalogue  Fossils  Cincinnati  Group,  p.  14. 

crosotus  Meek,  1873;  Pal.  Ohio,  vol.  1,  p.  165,  pi.  14,  figs.  10  a,  b. 

crosotus  Miller,  1874  ; Cincinnati  Quart.  Jour.  Sci.,  vol.  1,  p.  129. 

danai  Hall,  1862;  Geol.  Wisconsin,  vol.  1,  p.  432.  Niagara. 

Syn.,  Acidaspis  ula  (Wincliell  and  Marcy)  Hall,  20tli  Rept.  New  York  State  Cab. 
Nat.  Hist.,p.  389. 

danai  Hall,  1867;  20tli  Rept.  New  York  State  Cab.  Nat.  Hist.,  p.  333,  pi.  21, 

figs.  8,  9. 

danai  Hall,  1870 ; 20th  Rept.  New  York  State  Cab.  Nat.  Hist.,  p.  423,  pi.  21,  figs. 

8,  9 (rev.  ed.). 

[ Terataspis ] eriops  Hall,  1876;  Illus.  Devonian  Foss.  Crust.,  pi.  19,  figs.  4-7,10, 

11,  12.  (See  Lichas  ( Conolichas ) eriops  Hall.) 

fimbriata  Hall,  1879;  Description  of  New  Species  from  the  Niagara  Group,  p. 

20.  Niagara. 

fimbriata  Hall,  1882;  Trans.  Albuny  Inst.,  vol.  10,  p.  76. 

. 87 


88 


A BIBLIOGRAPHY  OF  PALEOZOIC  CRUSTACEA. 


[bull.  63. 


Acidaspis  flxnbriata  Hall,  1883;  lltli  Rept.  Geol.  Nat.  Hist.  Indiana,  p.  334,  pL  33, 
fig.  11. 

[ Terataspis ] grandis  Hall,  1870;  Ulus.  Devonian  Foss.  Crust.,  pi.  17,  figs.  1-8; 

pi.  18,  figs.  1-4.  (See  Licha.s  ( Terataspis ) grandis  Hall.) 

lialli  Shumard,  1855 ; 1st  and  2d  Rept.  Geol.  Survey  Missouri,  pt.  2,  p.  200,  pi.  B, 

figs.  7 a.  lb,  c.  Trenton. 

[ Discranurus ] harnata  Conrad,  1841;  5th  Ann.  Rept.  Pal.  Dept.  New  York  Geol. 

Survey,  p.  48,  pi.  1,  fig.  1.  Lower  Helderberg. 

[ Discranurus ] hamata  Hall,  1862;  15th  Rept.  New  York  State  Cab.  Nat.  Hist., 

pi.  2,  fig.  1.  Republicatiou  of  pi.  2,  5th  Ann.  Rept.  Pal.  Dept.  New  York  Geol. 
Survey. 

hamafa  Hall,  1859;  Pal.  New  York,  vol.  3,  p.  371,  pi.  79,  figs.  15-19. 

hamata  Meek  and  Worthen,  1868;  Geol.  Survey  Illinois,  vol.  3,  p.  390,  pi.  7,  fig.  17. 

horani  Billings,  1857;  Geol.  Survey  Canada,  p.  341.  Trenton. 

horani  Billings,  1863;  Geol.  Survey  Canada,  p.  190,  fig.  190. 

ida  Winchell  and  Marcy,  1865;  Mem.  Boston  Soc.  Nat.  Hist.,  vol.  1,  p.  106,  pi.  3, 

fig.  13. 

o’nealli  Miller,  1875;  Cincinnati  Quart.  Jour.,  vol.  2,  p.  86,  fig.  9.  Hudson. 

ortoni  Foerste,  1887 ; Bull.  Denison  Univ.,  vol.  2,  p.  90,  pi.  8,  fig.  1. 

parvula  Walcott,  1877 ; Advanced  sheets  31st  Rept.  New  York  State  Mus.,  p.  16. 

Trenton. 

parvula  Walcott,  1879  ; 31st  Rept.  New  York  State  Mus.,  p.  69. 

romingeri  Hall,  1888;  Pal.  New  York,  vol.  7,  pp.  71,224,  pi.  16  b,  figs.  15-18. 

Hamilton. 

spiniger.  .,(Seo  Bathyurus  spiniger.) 

trentonensis  Hall,  1847 ; Pal.  New  York,  vol.  1,  p.  240,  pi.  64,  figs.  4 af. 

Trenton. 

trentonensis  Emmons,  1855  ; American  Geology,  vol.  1,  pt.  2,  p.  216,  fig.  73. 

tuberculatus  Conrad,  1840;  3d  Ann.  Rept.  Pal.  Dept.  New  York  Geol.  Survey, 

p.  205.  # Lower  Helderberg. 

Syn.,  Acantholoma  Conrad,  1840;  3d  Ann.  Rept.  Pal.  Dept.  New  York  Geol.  Sur- 
vey, p.  205,  fig.  3. 

Acantholoma  spinosa  Conrad,  4th  Ann.  Kept.  Pal.  Dept.  New  York  Geol. 
Survey,  p.  39,  pi.  1,  fig  3. 

tuberculatus  Hall,  1859;  Pal.  New  York,  vol.  3,  p.  368,  pi.  79,  figs.  1-14. 

tuberculatus  Hall,  1861 ; 15th  Rept.  New  York  State  Cab.  Nat.  Hist.,  pi.  2,  fig.  3. 

Actinurus  De  Castelnau,  1843;  Sil.  Syst.  de  PAm6r.,  p.  21.  (See  Lichas  boltoni.) 
Aglaspis  Hall,  1862 ; Canadian  Naturalist,  vol.  7,  p.  445,  figure.  Hall,  1863 ; 16th 
Rept.  New  York  State  Cab.  Nat.  Hist.,  p.  181. 

Type,  Aglaspis  harrandi  Hall. 

barrandi  Hall,  1863;  16th  Rept.  New  York  State  Cab.  Nat.  Hist.,  p.  181,  pi.  11, 

figs.  7-16.  Potsdam. 

eatoni  Whitfield,  1880;  Ann.  Rept.  Geol.  Survey  Wisconsin,  p.  52.  Potsdam. 

eatoni  Whitfield,  1882 ; Geol.  Wisconsin,  vol.  4,  p.  192,  pi.  10,  fig.  11. 

Agnostus  Brongniart,  1822;  Hist.  Nat.  Crust.  Foss.,  p.  38. 

Type,  Agnostus pisiformis,  idem.,  p.  38,  pi.  4,  figs.  4 a,  4 b. 

Syn.,  Battus  Dalman,  1826;  Palsead.,  p.  33. 

Trinodus  McCoy,  1846 ; Sil.  Foss.  Ireland,  p.  56. 

Phalacroma  Corda  (in  part),  1847 ; Prodr.,  p.  158. 

Mcsosphcniscus  Corda,  1847 ; Prodr.,  p.  46  ( Agnostus  integer ). 

Diplorrhina  Corda,  1847 ; Prodr.,  p.  46. 

Condglopgge  Corda,  1847 ; Prodr.,  p.  50  (Agnostus  rex). 

Lejopyge  Corda,  1847 ; Prodr.,  p.  51  (Agnostus  Icevigatus). 

Arlhrorhachis  Corda,  1847  ; Prodr.,  p.  114  (Agnostus  tardus ). 

Pcronopsis  Corda,  1847;  Prodr.,  p.  115  (Agnostus  interger). 

. Pleuroctenium  Corda,  1847;  Prodr.,  p.  lift  (Agnostus  grannlatus). 


V0GDE8.] 


CATALOGUE  OF  TRILOBITES. 


89 


Agnostus  acadicus  Hartt,  1868  ; Acadian  Geology,  p.  655,  fig.  229  (3d  ed.).  St.  John. 
Syn.,  Similis  Hartt,  1868;  Acadian  Geology,  p.  656  (3d  ed.). 

Similis  Hartt  (Walcott),  1884 ; Bull.  U.  S.  Geol.  Survey,  No.  10,  p.  22. 

acadicus  Walcott,  1884;  Bull.  U.  S.  Geol.  Survey,  No.  10,  p.  22,  pi.  2,  figs.  2, 2 

a,  c. 

americauus  Billiugs,  1860 ; Canadian  Naturalist,  vol.  5,  p.  302,  fig.  1.  Quebec. 

americanus  Billings,  1865  ; Pal.  Foss.,  vol.  1,  p.  395,  fig.  372. 

bidens  Meek,  1873 ; 6th  Ann.  Rept.  U.  S.  Geol.  Survey  Territories,  p.  463. 

Potsdam. 

bidens  Walcott,  1884  ; Pal.  Eureka  Dist.,  Mon.  U.  S.  Geol.  Survey,  vol.  8,  p.  26, 

pi.  9,  figs.  13,  13  a. 

canadensis  Billings,  1860 ; Canadian  Naturalist,  vol.  5,  p.  304,  fig.  3.  Quebec. 

canadensis  Billings,  1865  ; Pal.  Foss.,  vol.  1,  p.  397,  fig.  374. 

coloradoensis  Shumard,  1861 ; Am.  Jour.  Sci.,  2d  series,  vol.  32,  p.  218. 

Potsdam. 

communis  Hall  and  Whitfield,  1877 ; U.  S.  Geol.  Expl.  40th  Par.,  vol.  4,  p.  228, 


pi.  1,  figs.  28,  29.  Potsdam. 

communis  Walcott,  1884;  Pal.  Eureka  Dist.,  Mon.  U.  S.  Geol.  Survey,  vol.  8, 

p.  27. 

disparlis  Hall,  1863;  16th  Rept.  New  York  State  Cab.  Nat.  Hist.,  p.  179,  pi.  10, 

figs.  25-27.  Potsdam. 

fabius  Billings,  1865;  Pal.  Foss.,  vol.  1,  p.  298,  fig.  289.  Quebec. 

glabba  Billings,  1865 ; Pal.  Foss.,  vol.  1,  p.  297,  fig.  288.  Quebec. 

interstrictus  White,  1874;  Prelim.  Rept.  Invert.  Foss.,  p.  7.  Potsdam. 


interstrictus  White,  1877 ; U.  S.  Geog.  and  Geol-  Survey  W.  100th  Meridian,  p. 

38,  pi.  2,  figs.  5 a,  5 b. 

interstrictus  Walcott,  1886;  Bull.  U.  S.  Geol.  Survey,  No.  30,  p.  149,  pi.  16, 

figs.  6, 6 a. 

interstrictus  Walcott,  1888  ; Am.  Jour.  Sci.,  3d  series,  vol.  36,  p.  166. 

sp.?  Rominger,  1887;  Proc.  Acad.  Nat.  Sci.  Phila.,  p.  18. 

josepha  Hall,  1863;  16th  Rept.  New  York  State  Cab.  Nat.  Hist.,  p.  178,  pi.  6, 

figs.  54, 55.  Potsdam. 

lobatus  Hall.  (See  Microdiscus  lobatus.) 

maladensis  Meek,  1873 ; 6th  Annual  Rept.  U.  S.  Geol.  Survey  Territories,  p.  464. 

Calciferous. 

neon  Hall  and  Whitfield,  1877 ; U.  S.  Geol.  Expl.  40th  Par.,  vol.  4,  p.  229,  pi.  1, 

figs.  26,27.  Potsdam. 

neon  Walcott,  1884  ; Pal.  Eureka  Dist.,  Mon.  U.  S.  Geol.  Survey,  vol.  8,  p.  27. 

nobilis  Ford,  1872 ; Am.  Jour.  Sci.,  3d  series,  vol.  3,  p.  421,  figs.  1,2.  Postdam. 

nobilis  Walcott,  1886;  Bull.  U.  S.  Geol.  Survey,  No.  30,  p.  150,  pi.  16,  fig.  7. 

orion  Billings,  1860;  Canadian  Naturalist,  vol.  5,  p.  304,  fig.  2.  Quebec. 

orion  Billings,  1865;  Pal.  Foss.,  vol.  1,  p.  397,  fig.  393 

orion  Shnrnard,  1863;  Trans.  Acad.  Sci.  St.  Louis,  vol.  2,  p.  105. 

parilis  Hall,  1863 ; 16th  Rept.  New  York  State  Cab.  Nat.  Hist.,  p.  179,  pi.  11,  figs. 

23, 24.  Potsdam. 

prolongus  Hall  and  Whitfield,  1877  ; U.  S.  Geol.  Expl.  40th  Par.,  vol.  4,  p.  230, 

pi.  1,  figs.  30, 31.  Potsdam. 

prolongus  Walcott,  1884  ; Pal.  Eureka  Dist.,  Mon.  U.  S Geol.  Survey,  vol.  8,  p.  28. 

richmondensis  Walcott,  1884;  Pal.  Eureka  Dist.,  Mon.  U.  S.  Geol.  Survey,  vol. 

8,  p.  24,  pi.  9,  fig.  10.  Cambrian. 

seclurus  Walcott,  1884  ; Pal.  Eureka  Dist.,  Mon.  U.  S.  Geol.  Survey,  vol.  8,  p.  25, 

pi.  9,  fig.  14.  Cambrian. 

similis  Hartt.  (See  Agnostus  acadicus.) 

tumidosus  Hall  and  Whitfield,  1877;  U.  S.  Geol.  Expl.  40th  Par.,  vol.  4,  p.  231, 

pi.  1,  fig.  32.  Potsdam. 


90 


A BIBLIOGRAPHY  OF  PALEOZOIC  CRUSTACEA. 


I BULL.  63. 


Agraulos  Corda,  1847;  Prodr.,  p.  23. 

Typo,  Arionellus  certicephalus  Barrande. 

Syn.,  Avion  Barrande,  1846;  Notice  Prdlim.,  p.  13. 

Ellipsocephalus  Barrande,  1846;  Notice  Prdlim.,  p.  12  (not  Ellipsocephalus 
Zenker)  or  ( Elliptocephalus  Emmons). 

Arionellus  Barrande,  1852;  Syst.  Sci.  Boheme,  p.  404. 

affinis  Billings,  1874;  Pal.  Foss.,  vol.  2,  p.  72.  Potsdam. 

affinis  Matthew,  1886;  Traus.  Royal  Soc.  Canada,  vol.  2,  p.  153,  figs,  2, 2 a,  b. 

[ Arionellus ] bipunctatus  Shumard,  1863;  Trans.  Acad.  Sci.  St.  Louis,  vol.  2,  p. 

101.  Potsdam. 

[ Arionellus ] bipunctatus  Hall,  1863 ; 16tk  Kept.  New  York  State  Cab.  Nat. 

Hist.,  p.  169,  pi.  7,  figs.  50-57. 

[ Arionellus  ( Agraulos )]  convexus  Whitfield,  1878;  Ann.  Rept.  Geol.  Survey 

Wisconsin,  1877,  p.  57.  Potsdam. 

[ Arionellus']  convexus  Whitfield,  1882;  Geol.  Wisconsin,  vol.  4,  p.  190,  pi.  1, 

fig.  17. 

[ Arionellus ] cylindricus  Billings,  1860;  Canadian  Naturalist,  vol.  5,  p.  314,  fig. 

14.  Quebec. 

[ Arionellus']  cylindricus  Billings,  1865;  Pal.  Foss.,  vol.  1,  p.  406,  fig.  385.  (See 

Ptychaspis  cylindricus.) 

? globosus  Walcott,  1884 ; Pal.  Eureka  Dist.,  Mon.  U.  S.  Geol.  Survey,  vol.  8, 

p.  61,  pi.  9,  fig.  23.  Cambrian. 

oweni  Meek  and  Hayden,  1861;  Proc.  Acad.  Nat.  Sci.  Phila.,  1861,  p.  436. 

Potsdam. 

The  s*pecies  was  also  referred  to  the  genera  Arionellus  and  Crepicephalus. 

[Arionellus ] oweni  Meek  and  Hayden,  1862;  Atn.  Jour.  Sci.,  2d  series,  vol.  33, 

p.  74. 

[ Arionellus ] oweni  Meek  and  Hayden ; Pal.  Upper  Missouri,  p.  9,  figs,  a,  b,  c, 

pi.  1,  fig.  4. 

Referred  by  Walcott,  1884,  Pal.  Eureka  Dist.,  Mon.  U.  S.  Geol.  Survey,  vol. 
8,  p.  55,  pi.  10,  to  Ptychoparia  oweni. 

[Arionellus  ( Bathyurus )]  planus  Shumard,  1861;  Am.  Jour.  Sci.,  2d  series,  vol. 

32,  p.  219.  Potsdam. 

[ Arionellus ] pustulatus  Walcott,  1877 ; Advanced  sheets  31st  Rept.  New  York 

State  Mus.  Nat.  Hist.,  p.  15.  Chazy. 

[Arionellus']  pustulatus  Walcott,  1877;  31st  Rept.  New  York  State  Mus.  Nat. 

Hist.,  p.  68. 

[ Arionellus ] quadrangularis  Whitfield,  1884;  Bull.  Mus.  Nat.  Hist.  New  York, 

vol.  1,  p.  147,  pi.  14,  fig.  8.  Potsdam. 

quadrangularis  Walcott,  1884  ; Bull.  U.  S.  Geol.  Survey,  No.  10,  p.  48,  pi.  7,  fig.  1. 

socialis  Billings,  1874;  Pal.  Foss.,  vol.  2,  p.  71,  fig.  40.  Potsdam. 

socialis  Matthew,  1886;  Trans.  Royal  Soc.  Canada,  vol.  2,  p.  151,  fig.  1,  1 a,  b. 

strenuus  Billings,  1874;  Pal.  Foss.,  vol.  2,  p.  71,  fig.  41.  Potsdam. 

strenuus  Matthew,  1886 ; Trans.  Royal  Soc.  Canada,  vol.  2,  p.  153,  figs.  3,  3 a,  b. 

subclavatus  Billings.  (See  Ptychaspis  subclavatus.) 

[ Arionellus  ( Bathyurus )]  texanus  Shumard,  1861 ; Am.  Jour.  Sci.,  2d  series,  vol. 

32,  p.  218.  Potsdam. 

[ Arionellus]  tripunctatus  Whitfield,  1876;  Rept.  Recon.  Upper  Missouri,  p.  141, 

pi.  1,  figs.  3-5.  Potsdam. 

[Bathyurus?]  woosteri  Whitfield,  1878;  Ann.  Rept.  Geol.  Survey  Wisconsin, 

1877,  p.  56.  Potsdam. 

[Bathyurus?]  woosteri  Whitfield,  1882;  Geol.  Wisconsin,  vol.  4,  p.  189,  pi.  1, 

figs.  19-21. 

Amphion  Pander,  1830 ; Beitriige  zur  Geol.  russischen  Reiches,  p.  139. 

Type,  Amphion  fisclieri  Eichwald. 


VOODES.j 


CATALOGUE  OF  TRlLOBITES 


91 


Quebec. 

Chazy. 


Quebec. 

Quebec. 

Quebec. 


Quebec. 


166, 
Trenton. 
Cbazy. 

Quebec. 

Quebec. 

Quebec. 

Quebec. 


Amphion  barrandi  Billings,  1865;  Pal.  Foss.,  vol.  l,p.  288,  fig.  277. 

— - canadensis  Billings,  1859;  Can.  Nat.,  vol.  4,  p.  381,  fig.  12,  a,  b. 

canadensis  Billings,  1863  ; Gcol.  Survey  Canada,  p.  133,  fig.  69. 

canadensis  Billings,  1865;  Pal.  Foss.,  vol.  1,  p.  288,  fig.  278. 

convexus  Billings,  1865 ; Pal.  Foss.,  vol.  1,  p.  322. 

insularis  Billings,  1865;  Pal.  Foss.,  vol.  1,  p.  290. 

julius  Billings,  1865;  Pal.  Foss.,  vol.  1,  p.  290,  fig.  279. 

matutina  Hall,  1863;  16th  Kept.  New  York  State  Cab.  Nat.  Hist.,  p.  222,  pi.  5 a, 

fig.  6.  Potsdam. 

multisegment atus.  (See  Encrinurus  multisegmentatus.) 

nevadensis  Walcott,  1884;  Pal.  Eureka  Dist.  Mon.  U.  S.  Geol.  Survey,  vol.  8,  p. 

94,  pi.  12;  fig.  13.  Pogonip. 

salteri  Billings,  1861 ; Canadian  Naturalist,  vol.  6,  p.  322,  fig.  6.  Calciferous. 

salteri  Billings,  1865 ; Pal.  Foss.,  vol.  1,  p.  352,  fig.  399. 

westoni  Billings,  1865 ; Pal.  Foss.,  vol.  1,  p.  321,  fig.  307. 

Ampyx  Dalman,  1826;  Palaead.,  p.  53  (German  edition). 

Type,  Ampyx  nasuta  Dalman. 

americanus  Safford  and  Yodges,  1889;  Proc.  Phila.  Acad.  Nat.  Sci.,  p 

figure. 

halli  Billings,  1861 ; Pal.  Foss.,  vol.  1,  p.  24,  figs.  25,  a,  b,  c. 

halli  Billings,  1862;  Geol.  Survey  Vermont,  vol.  2,  p.  959,  fig.  365. 

laeviusculus  Billings,  1865;  Pal.  Foss.,  vol.  1,  p.  295,  fig.  285. 

tiormalis  Billings,  1865;  Pal.  Foss.,  vol.  1,  p.  295,  fig.  286. 

rustilius  Billings,  1865  ; Pal.  Foss.,  vol.  1,  p.  296. 

semicostatus  Billings,  1865;  Pal.  Foss.,  vol.  1,  p.  297,  fig.  287. 

Angelina  Salter,  1864  ; Mem.  Geol.  Survey  United  Kingdom,  decade  xi,  pi.  7. 

Type,  Angelina  sedgwicki  Salter. 

hitchcocki  Whitfield,  1884;  Bull.  Am.  Mus.  Nat.  Hist.,  New  York,  vol.  1,  p. 

148, pi.  14,  fig.  13.  (See  Frotypus  hitchcocki.)  Potsdam. 

Anomocare  Angelin,  1852  ; Palseont.  Scand.,  p.  24. 

Type,  Anomocare  aculeatus  Ang.,  pi.  18,  fig.  6. 

[?  Conoceph.]  depressus  Shumard,  1861;  Am.  Jour.  Sci.,  2d  series,  vol.  32,  p. 

219.  Potsdam. 

[ Lonchocephus]  hamulus  Owen,  1852;  Geol.  Survey  Wisconsin,  Iowa,  and  Min- 
nesota, p.  576,  pi.  1 a,  figs.  8-12.  Potsdam. 

undet.  Trilobite,  Owen,  1848 ; Geol.  Reconnoissance  Chippewa  Land  Dist.,  p. 

15,  pi.  7,  fig.  5. 

[ Conocephalites]  hamulus  Shumard,  1863;  Acad.  Sci.  St.  Louis,  vol.  2,  p.  104. 

[ Conoceplmlites]  hamulus  Hall,  1863;  16th  Kept.  New  York  State  Cab.  Nat. 

Hist.,  p.  166,  pi.  7,  figs.  43,44;  pi.  8,  figs.  25,26. 

hamulus  Dames,  1884  ; China  (Richthofen),  vol.  4,  p.  24. 

[Conocephalites]  patersoni  Hall,  1863;  Rept.  New  York  State  Cab.  Nat.  Hist.,  p. 

159,  pi.  7,  figs.  45,  46.  Potsdam. 

patersoni  Dames,  1884 ; China  (Richthofen),  vol.  4,  p.  24. 

? parvum  Walcott,  1884  ; Pal.  Eureka  Dist.,  Mon.  U.  S.  Geol.  Survey,  vol.  8,  p. 

59,  pi.  9,  fig.  17.  * Cambrian. 

? parvum  Walcott,  1886;  Bull.  U.  S.  Geol.  Survey,  No.  30,  p.  209,  pi.  25, 

fig.  1. 

[Crcpicephalus  ?]  wisconsensis  Owen,  1852;  Rept.  Geol.  Survey  Wisconsin, 

Iowa,  and  Minnesota,  pi.  1,  fig.  13.  (The  upper  figure  only  ; the  other  figured 
specimen  belongs  to  Dikelocephalus  granulosus.) 

[Crepicephalu8]  wisconsensis  Shumard,  1863;  Trans.  Acad.  Sci.  St.  Louis,  vol. 

2,  p.  103. 


92 


A BIBLIOGRAPHY  OF  PALEOZOIC  CRUSTACEA. 


[BULL.  63. 


Anomocare  [ Crepicephalus}  wisconsensis  Hall,  1863;  16tli  Rept.  New  York  State 
Cab.  Nat.  Hist.,  p.  164,  pi.  7,  figs.  39-41 ; pi.  8,  tigs.  22, 23, 24, 27, 28. 

Syn.,  Dikelocephalus  latifrons  (Shumard)  Hall,  1863;  16tli  Rept.  New  York  State 
Cab.  Nat.  Hist.,  p.  165,  pi.  7,  fig.  40. 

wisconsensis  Dames,  1884;  China  (Richthofen),  vol.  4,  p.  24.  Potsdam. 

Anopolenus  Salter,  1864;  Geol.  Mag.,  vol.  1,  jj.  236. 

Type,  Anopolenus  henrici  Salter ; Quar.  Jour.  Geol.  Soc.  London,  vol.  20,  p.  236,  pi. 
13,  figs.  4,  5.  (See,  also,  Anopolenus  salteri  Hicks ; same  journal,  vol. 
21,  p.  478,  pi.  , fig.  1. 

venustus  Billings,  1874 ; Pal.  Foss.,  vol.  2,  p.  73,  fig.  42.  Potsdam. 

Arethusina  Barrande,  1852 ; Syst.  Sii.  Boheme,  vol.  1,  p.  493. 

Type,  Arethusina  konincki  Barrande. 

americana  Walcott,  1884;  Pal.  Eureka  Dist.,  Mon.  U.  S.  Geol.  Survey,  vol.  8,  p. 

62,  pi.  9,  fig.  27.  Cambrian. 

Arges.  (See  Lichas.) 

Arges,  subgenus  Lichas,  Hall  and  Clarke,  1888  ; Pal.  New  York,  vol.  7,  p.  lx. 

phlyctanodes  Green.  (See  Lichas  phlyctanodes. ) 

arionellus.  (See  Agraulos.) 

Asaphiscus  Meek,  1873 ; 6th  Ann.  Rept.  U.  S.  Geol.  Survey  Territories,  p.  485  (foot- 
note). 

\_Bathyurellus  ( Asaphiscus )]  bradleyi  Meek,  1873;  6th  Ann.  Rept.  U.  S.  Geol. 

Survey  Territories,  p.  484.  Cambrian. 

bradleyi  Meek,  1873;  6th  Ann.  Rept.  U.  S.  Geol.  Survey  Territories,  p.  485. 

wkeeleri  Meek;  1873;  6th  Rept.  U.  S.  Geol.  Survey  Territories,  p.  485  (foot- 
note). • Cambrian. 

wheeleri  White,  1875;  Geog.  and  Geol.  Survey  West  100th  Meridian,  vol.  4,  p.  43, 

pi.  2,  figs.  1 a-f. 

wheeleri  Walcott,  1886;  Bull.  U.  S.  Geol.  Survey,  No.  30,  p.  220,  pi.  31,  figs.  3,3  a.* 

Asaphus  Brongniart,  1822;  Hist.  Nat.  Crust.  Foss.,  p.  18,  pi.  2,  fig.  1 a,  b. 

Type,  Asaphus  expansus  Linn6. 

Syn.,  Cryptonymus,  Eichwald,  1825;  (in  part)  not  Cryptonymus  Eichwald,  1840. 
Isotelus  De  Kay,  1822;  Annals  Lyceum  Nat.  Hist.  New  York,  vol.  1,  p.  174. 
Hemicrupturus  Green,  1832;  Mon.  Tril.  North  America,  p.  20. 

acantholeurus.  (See  Dalmanites  acantholeurus.) 

alacer  Billings,  1866;  Catalogue  Sil.  Foss.  Anticosti,  p.  26,  fig.  9. 

aspectans.  (See  Dalmanites  aspectans.) 

astragalotes  Green,  1834;  Am.  Jour.  Sci.,  1st  series,  vol.  25,  p.  335. 

astragalotes  Green,  1835;  Suppl.  Mon.  Tril.  N.  A.,  p.  11,  cast  37. 

Probably  Phacops  rana  Green. 

barrandi.  (See  Ogygia  barrandi.) 

canadensis  Chapman,  1856;  Canadian  Jour.,  vol.  1,  p.  482.  Utica  Slate. 

canadensis  Chapman,  1858;  Canadian  Jour.,  vol.  2,  p.  47. 

canadensis  Chapman,  1858;  Canadian  Jour.,  vol.  3,  p.  230,  figure. 

canadensis  Chapman,  1859;  Canadian  Jour.,  vol.  4,  p.  1,  figure. 

canadensis  Chapman,  1859;  Annals  Nat.  Hist.,  3d  series,  vol.  2,  p.  9,  fig.  1. 

canadensis  Billings,  1863 ; Geol.  Survey  Canada,  p.  204,  fig.  201. 

From  a personal  study  of  the  species  collected  on  the  Georgian  Bay,  Canada,  " 
I am  inclined  to  refer  Asaphus  halli  and  A.  hincksii  to  Asaphus  canadensis 
Chapman. 

[ Isotelus ] canalis  Conrad  MSS.  Chazy.  } 

[ Isotelus *]  canalis  Hall,  1847;  Pal.  New  York,  vol.  1,  p.  25,  pi.  4 bis,  figs.  17-19. 

canalis  Billings,  1865;  Pal.  Foss.,  vol.  1,  p.  255;  also  p.  352,  fig.  340  (not  Con- 
rad sp.). 

canalis  Billings,  1862;  Geol.  Vermont,  vol.  1,  p.  299,  pi.  12,  fig.  5. 

This  species  is  probably  Asaphus  platycephalus. 


CATALOGUE  OF  TRJLOBITES. 


vogdes.  | 


93 


Asaphus  canalis  Whitfield,  1886;  Bull.  Am.  Mus.  Nat.  Hist.,  New  York,  vol.  1,  p. 
336,  pi.  34,  figs.  1-8. 

canalis  Whitfield,  1889 ; Bull.  Am.  Mus.  Nat.  Hist.,  New  York,  vol.  2,  p.  64, 

pis.  11, 12. 

caribouensis  Walcott,  1884;  Pal.  Eureka  Dist.,Mon.  U.  S.  Geol.  Survey,  vol.  8, 

p.  98,  pi.  12,  figs.  7-7  a,  b.  Pogonip. 

caudaius.  (See  Dalmanites  limulurus.) 

cordieri.  (See  Dalmanites  limulurus.) 

corycoeus.  (See  Proetus  corycceus.) 

crypturus.  (See  Homalonotus  crypturus.) 

curiosus  Billings,  1865;  Pal.  Foss.,  vol.  1,  p.  318,  fig.  305.  Quebec. 

? curiosus  Walcott,  1884;  Pal.  Eureka  Dist.,  Mon.  U.  S.  Geol.  Survey,  vol.  8,  p. 

98,  pi.  12,  fig.  15. 

denticulatus.  (See  Dalmanites  denticulatus. ) 

ditmarsice  Houeyman,  1879 ; Proc.  Nova  Scotia  Inst.  Nat.  Sci.,  vol.  5,  p.  18. 

(See  Homalonotus  crypturus  Green.)  Clinton? 

duirus  Green,  1839;  Am.  Jour.  Sci.,  1st  series,  vol.  37,  p.  40.  Hudson. 

edicardi.  (See  Dalmanites  limulurus.) 

emoryi  Hall,  1857 ; Rept.  U.  S.  Mexican  Boundary  Survey,  vol.  1,  pi.  20,  fig.  5. 

Not  defined. 

sxtans.  (See  Bathyurus  extans.) 

gigas.  (See  Asaphus  platycephalus.) 

[Megalaspis? ] goniocercus  Meek,  1873 ; 6th  Ann.  Rept.  U.  S.  Geol.  Survey  Ter- 
ritories, p.  480.  Quebec. 

goniurus  Billings,  1860;  Canadian  Naturalist,  vol.  5,  p.  324.  Quebec. 

goniurus  Billings,  1865;  Pal.  Foss.,  vol.  l,p.  415. 

halli.  (See  Cryphaeus  boothi.) 

halli  Chapman,  1858;  Annals  Nat.  Hist.,  3d  series,  vol.  2,  p.  14,  fig.  2. 

Trenton  and  Utica. 

halli  Chapman,  1858;  Canadian  Jour.,  2d  series,  vol.  3,  p.  236,  figure. 

This  species  is  the  same  as  Asaphus  canadensis  Chapman. 

hincksii  Chapman,  1859 ; Canadian  Jour.  Industry,  Sci.  and  Arts,  vol.  4,  p.  2, 

figure.  (See  Asaphus  canadensis  Chapman.)  Utica. 

homalononotoides  Walcott,  1877 ; Advanced  sheets  31st  Rept.  New  York  State 

Mus.  Nat.  Hist.,  p.  20.  Trenton. 

homalononotoides  Walcott,  1879  ; 31st  Rept.  New  York  State  Mus.  Nat.  Hist., 

p.  71. 

homalononotoides  Whitfield  (not  Walcott),  1882;  Geol.  Wisconsin,  vol.  4,  p.  237. 

(See  Asaphus  triangulatus.) 

huttoni  Billings,  1865;  Pal.  Foss.,  vol.  1,  p.  271,  fig.  256.  Quebec. 

illsenoides  Billings,  1860 ; Canadian  Naturalist,  vol.  5,  p.  323. 

illeenoides  Billings,  1865 ; Pal.  Foss.,  vol.  1,  p.  414. 

[Isotelus]  iowensis  Owen,  1852;  Rept.  Geol.  Survey  Wisconsin,  Iowa,  and  Min- 
nesota, p.  577,  pi.  2 a,  figs.  1-7.  Trenton. 

laticostatus.  (See  Dalmanites  anchiops.) 

? latimarginata  Hall,  1847 ; Pal.  New  York,  vol.  1,  p.  253,  pi.  66,  figs.  4 a,  b. 

Utica. 

limulurus.  (See  Dalmanites  limulurus.) 

marginalis  Hall,  1847 ; Pal.  New  York,  vol.  1,  p.  24,  pi.  4 his,  fig.  15.  Chazy. 

marginalis  Emmons,  1855;  Am.  Geology,  vol.  1,  pt.  2,  p.  235,  pi.  3,  fig.  16. 

- — llsotelns ] maximus  Locke,  1838;  2d  Ann.  Rept.  Geol.  Survey  Ohio,  p.  246,  figs. 

Trenton  and  Hudson. 

Syn.,  Isotelus  megistos  Locke,  1841;  Trans.  Am.  Assoc.  Geol.  Nat.,  p.  221,  pi.  6. 
Isoteius  megistos  Locke,  1842;  Am.  Jour.  Sci.,  1st  series,  vol.  42,  p.  366,  pi.  3. 


94 


A BIBLIOGRAPHY  OP  PALEOZOIC  CRUSTACEA. 


[hull.  03. 


Syn.,  Isotelus  megistos  Meek,  1873;  Pal.  Ohio,  vol,l,  p.  157,  pi.  14,  fig.  13. 

Isotelus  megistos  Miller,  1874,  Cincinnati  Quart.  Jour.  Sci.,  vol.  1,  p.  137. 
Asaphus  megistos  Walcott,  1884;  Science,  Marcli  7,  fig.  1,  vol.  3,  p.  200. 
Asaphus  megalopthalmus  Troost,  1840;  5tli  Geol.  Rept.  Tennessee,  p.  57. 

Trenton  ? 

micropleurus  Green,  1835;  Suppl.  Mon.  Tril.  North  America,  p.  21,  cast  No.  41. 

micrurus.  (See  Dalmanites  micrurus.) 

morrisi  Billings,  1865;  Pal.  Foss.,  vol.  1,  p.  272,  fig.  257,  Syn.  to  Asaphus  huttoni 

Billings. 

murchisoni  Castelnau,  Syn.  to  Asaphus  platycephalus  Stokes. 

myrmecophorus.  (See  Dalmanites  myrmecophorus. ) 

nasutus.  (See  Dalmanites  nasutus.) 

? nodostriatus  Hall,  1847;  Pal.  New  York,  vol.  1,  p.  248,  pi.  Cl,  figs.  1 a,  b.  (See 

Bathyurus  extans  Hall.) 

notans  Billings,  1866 ; Catalogue  Silurian  Foss.  Anticosti,  p.  25,  fig.  8. 

Compare  Asaphus  maximus  Locke. 

? obtusus  Hall,  1847 ; Pal.  New  York,  vol.  1,  p.  24,  pi.  4 bis,  fig.  14.  Chazy. 

obtusus  Emmons,  1855 ; American  Geology,  vol.  2,  pt.  2,  p.  236,  pi.  3,  fig.  14. 

pelops  Billings,  1865 ; Pal.  Foss.,  vol.  1,  p.  317,  fig.  304.  Quebec 

platycephalus  Stokes,  1823 ; Trans.  Geol.  Soc.  London,  2d  series,  vol.  1,  p.  208, 

pi.  27.  Trenton. 

Syn.,  Isotelus  gigas  De  Kay,  1824;  Annals  Lyceum  Nat.  Hist.  New  York,  vol.  1,  p. 
176,  pi.  12,  fig.  1. 

Is  ot  el  us  planus  De  Kay,  1824;  Annals  Lyceum  Nat.  Hist.  New  York,  vol.  1, 
p.  1^8,  pi.  13,  fig.  7. 

Asaphus  gigas  Dalman,  1826;  Palsead.,p.  70. 

Asaphus  gigas  and  planus  Dalman,  1826  ; Palsead.,  p.  70. 

Isotelus  gigas  Green,  1832 ; Monthly  Am.  Jour.  Geol.,  p.  560. 

Isotelus  gigas  Green,  1832 ; Mon.  Tril.  N.  A.,  p.  71,  cast  21, 22. 

Isotelus  planus  Green,  1832;  Monthly  Am  Jour.  Geol.,  p.  560;  Mon.  Tril.  N. 
A.,  p.  68,  cast  23. 

Isotelus  stegops  Green,  1832;  Mon.  Tril.  N.  A.,  p.  71;  cast  26,  27. 

Brongniartia  isotelea  Eaton,  1832;  Geological  Text  Book,  p.  33,  pi.  2,  fig.  22. 

platycephalus  Broun,  1835;  Lethaea  Geogn.,  vol.  1,  p.  115,  pi.  9,  fig.  8. 

Syn.,  Isotelus  gigas  Milne-Edwards,  1840 ; Crust.,  vol.  3,  p.  298. 

platycephalus  Buckland,  1840 ; Bridgw.  Treatise,  vol.  2,  p.  76,  pi.  63,  fig.  12. 

platycephalus  Burmeister,  1843;  Org.  Trilobites,  p.  110,  pi.  2,  fig.  12  (Ray  Soc. 

ed.,  1846). 

Syn.,  Isotelus  gigas  Portlock,  1843;  Geol.  Rept.  Londonderry,  p.  295,  pi.  7,  fig.  1; 
pi.  8,  fig.  1. 

Isotelus  planus  Portlock,  1843  ; Geol.  Rept.  Londonderry,  p.  295,  pi.  7,  figs. 
2, 3. 

Isotelus  gigas  Hall,  1847  ; Pal.  New  York,  vol.  1,  p.  231,  pis.  60-63. 

Isotelus  gigas  Emmons,  1855;  Am.  Geology,  vol.  1,  pt.  2,  p.  215,  pi.  16,  fig.  12. 

[ Isotelus ] platycephalus  Broun  and  Roemer,  1851-56;  Lethma  Geogn.,  vol.  1, 

p.  632,  pi.  9,  fig.  8 ; pi.  91,  fig.  5. 

platycephalus  Nieszkowski,  1857;  Mon.  Sil.  Ostseeprovinz,  Tril.,  p.  37. 

Syn.,  Isotelus  gigas  Rogers,  1858 ; Geol.  Survey  Pennsylvania, vol.  2,  p.  819,  fig.  610. 

platycephalus  Billings,  1863 ; Geol.  Survey  Canada,  p.  184,  fig.  183. 

Syn.,  Asaphus  ( Isotelus ) gigas  Salter,  1864 ; Mou.  Brit.  Tril.,  p.  161,  pi.  24,  figs..  1-5; 
pi.  25,  fig.  1 (var.). 

Asaphus  ( Isotelus ) gigas  Salter,  1864;  Mem.  Geol.  Survey  United  Kingdom, 
decade  xi,  pi.  3. 


VOGDES.] 


CATALOGUE  OF  TKILOBITES. 


95 


Asaphus  platycephalus  Billings,  1870  ; Quart.  Jour.  Geol.  Soc.  London,  vol.  26,  p. 
486,  pis.  31,  32. 

Syn.,  Isotelu3  gigas  Miller,  1874;  Cincinnati  Quart.  Jour.  Sci.,  vol.  l,p.  138. 

platyleurus  Green,  1837;  Am.  Jour.  Sci.,  1st  series,  vol.  32,  p.  169.  (SeeDal- 

manitis  platyleurus. ) 

polypleurus  Green,  1838;  Am.  Jour.  Sci.,  1st  series,  vol.  34,  p.  380. 

quadraticaudatus  Billings,  1865;  Pal.  Foss.,  vol.  1,  p.  273,  fig.  258.  Quebec. 

rcemingeri  Walcott,  1876;  28th  Kept.  New  York  State  Mus.  Nat.  Hist.,  p.  96. 

Trenton. 

selenurus.  (See  Dalmanites  selenurus.) 

stokesi.  (See  Froetus  stokesi.) 

susae  Calvin  ; MSS. 

susae  Whitfield,  1882;  Geol.  Wisconsin,  vol.  4,  p.  236,  pi.  5,  fig.  3 ; pi.  10,  fig.  8. 

Trenton. 

tetragonocephalus  Green,  1834 ; Am.  Jour.  Sci.,  1st  series,  vol.  25,  p.  135. 

tetragonocephalus  Green,  1835;  Suppl.  Mon.  Tril.  N.  A.,  p.  12,  cast  38. 

[ Paradoxides ] tetragonocephalus  Emmrich,  1839;  De  Tril.,  etc.,  p.  34. 

The  cast  issued  with  Dr.  Green’s  monograph  as  No.  38  may  be  the  same 
species  which  Dr.  Emmons  afterwards  described  as  Atops  trilineatus.  It  .has 
about  sixteen  segments  in  the  thorax,  also  obscure  nodes  along  the  axis.  The 
head  shows  the  occular  ridges  of  a Ptyclwparia,  whereas  the  segments  are  those 
characterise  of  the  Oleni.  It  is  too  imperfect  for  generic  classification. 

trentonensis.  (See  Lidias  trentonensis.) 

triangulatus  Whitfield,  1880 ; Ann.  Rept.  Geol.  Survey  Wisconsin,  1879,  p.59. 

Trenton. 

This  species  is  the  Asaphus  homalonotoides  of  the  Final  Report,  vol.  4,  p.  237, 

pi.  5,  fig.  4. 

? trimblii  Green,  1837 ; Acad.  Nat.  Sci.  Phila.,  Jour.,  vol.  7.  Niagara. 

trimblii  Green,  1837 ; Am.  Jour.  Sci.,  1st  series,  vol.  32,  p.  348. 

LOgygia ?]  vetustus  Hall,  1847 ; Pal.  N.  Y.,  vol.  1,  p.  227,  pi.  60,  fig.  1. 

Trenton  and  Hudson. 

? lOgygia ] vetustus  Emmons,  1855;  Am.  Geology,  vol.  1,  pt.  2,  p.  216,  fig.  72. 

[ Isotelus]  vigilans  Meek  and  Worthen,  1870  ; Proc.  Acad.  Nat.  Sci.  Phila.,  p.  53. 

Hudson. 

llsotelus]  vigilans  Meek  and  Worthen,  1875;  Geol.  Illinois,  vol.  6,  p.  491,  pi.  23, 

fig.  6. 

wisconsensis  Walcott,  1876;  28th  Rept.  N.  Y.  State  Mus.  Nat.  Hist.,  p.  97. 

Trenton. 

Aspidolites  Conrad,  1841 ; 4th  Ann.  Rept.  Pal.  Dept.  New  York  Geol.  Survey,  p.  48. 
Atops  Emmons,  1844  ; Taconic  System,  p.  20. 

Type,  Atops  trilineatus  Emmons. 

trilineatus  Emmons  1844  ; Taconic  System,  p.  20,  fig.  1,  pi.  2,  fig.  3.  Taconic. 

trilineatus  Emmons,  1847;  Nat.  Hist.  New  York,  Agriculture,  vol.  1,  p.  64,  fig.  8, 

pi.  14,  fig.  3. 

Syn.,  Cahjniene  beckii  Hall,  1847 ; Pal.  New  York,  vol.  1,  p.  252,  pi.  67,  figs.  4 a-4  e 
(not  Cahjniene  beckii  Green,  or  Atops  trilineatus  Emmons). 

trilineatus  Haldeman,  1848;  Am.  Jour.  Sci.,  2d  series,  vol.  5,  p.  107. 

trilineatus  Emmons,  1849;  Proc.  Am.  Assoc.  Adv.  Sci.,  1st  Meeting,  Phila.,  1848, 

pp.  16, 17. 

Syn.,  Calymenc  beckii  Fitch,  1849;  Trans.  Agric.  Soc.  New  York,  vol.  9,  p.  865 
(not  Calymene  beckii  Green). 

trilineatus  Emmons,  1855 ; Am.  Geology,  vol.  1,  pt.  2,  p.  115,  pi.  1,  fig.  16. 

Syn.,  Atops  punctatus  Emmons,  1860;  Manual  Geology,  p.  88,  fig.  71;  aiso  p. 

280. 


96 


A BIBLIOGRAPHY  OF  PALEOZOIC  CRUSTACEA. 


[bull.  63. 


Atops  trilineatus  Barrande,  1861 ; Ball.  Soc.  G6ol.  France,  2d  series,  vol.  18,  p.  269, 
pi.  5,  fig.  1. 

trilineatus  Barrande,  1861 ; Bull.  Soc.  G6ol.  France,  2d  series,  vol.  18,  p.  271,  pi. 

5,  fig.  3. 

[ Conocephalites  ( Atops )]  trilineatus  Ford,  1871;  Am.  Jour.  Sci.,  3d  series,  vol. 

2,  p.  33. 

[Conocephalites]  trilineatus  Ford,  1873 ; Am.  Jour.  Sci.,  3d  series,  vol.  6,  p.  135. 

[ Conocephalites  (Atops)]  trilineatus  Ford,  1879;  Am.  Jour.  Sci.,  3d  series,  vol.  9, 

p.  205. 

[ Triarthrus ] trilineatus  Miller,  1877  ; Catalogue  Am.  Pal.  Foss.,  p.  223. 

[Conocoryphe]  trilineatus  Ford,  1880;  Am.  Jour.  Sci.,  3d  series,  vol.  19,  p.  152. 

Syn.,  Triarthrus  beclci  Walcott,  1879;  Trans.  Albany  Inst.,  vol.  10,  p.  23. 

[ Ptycoparia ] trilineatus  Walcott,  1886;  Bull.  U.  S.  Geol.  Survey,  No.  30,  p.  203, 

pi.  27,  fig.  1 a-c. 

I Conocoryphe']  trilineatus  Walcott,  1887  ; Am.  Jour.  Sci.,  3d  series,  vol.  34,  p. 

197,  pi.  1,  fig.  7 a,  b. 

Bailiella  Matthew,  1884;  Trans.  Royal  Soc.  Canada,  vol.  1,  p.  124  (used  as  a subgenus 
to  Conocoryphe  ( Bailiella ) Baileyi). 

Barrandia  Hall,  1860;  13th  Rept.  New  York  State  Cab.  Nat.  Hist.,  p.  115  (not  Bar- 
randia  McCoy).  (See  Olenellus.) 

thompsoni.  (See  Olenellus  thompsoni.) 

v ennontana.  (See  Olenellus  vermontana  and  Mesonasis  vermontana.) 

Barrandia  McCoy,  1849;  Annals  Nat.  Hist.,  2d  series,  vol.  4,  p.  409. 

Type,  Barrandia  cordai  McCoy. 

? mccoyi  Walcott,  1884 ; Pal.  Eureka  Dist.,  Mon.  U.  S.  Geol.  Survey,  vol.  8,  p.  96, 

pi.  12,  fig.  5.  Pogonip. 

Bathynotus  Hall,  1860;  13th  Rept.  New  York  State  Cab.  Nat.  Hist.,  p.  117. 

Type,  Bathynotus  holopyga  Hall. 

\_Peltura  ( Olenus )]  holopyga  Hall,  1859;  12th  Rept.  New  York  State  Cab.  Nat. 

Hist.,  p.  61,  figure. 

[Peltura  ( Olenus )]  holopyga  Hall,  1859 ; Pal.  New  York,  vol.  3,  p.  528,  figure. 

Syn.,  Paradoxides?  quadrispinosus  Emmons,  1860;  Manual  Geology,  p.  80,  fig.  57. 
Paradoxides  ( Pagura ) quadrispinosus  Emmons,  1860;  Manual  Geology,  p. 
280,  fig.  57. 

holopyga  Hall,  1860;  13th  Rept.  New  York  State  Cab.  Nat.  Hist.,  p.  118,  figure. 

holopyga  Hall,  1861 ; Geol.  Vermont,  vol.  1,  p.  371,  pi.  13,  fig.  3. 

[Peltura  (Olenus)]  holopyga  Barrande,  1861 ; Bull.  Soc.  G6ol.  France,  2d  series, 

vol.  18,  p.  278,  pi.  5,  figs.  9, 10. 

holopyga  Walcott,  1886;  Bull.  U.  S.  Geol.  Survey,  No.  30,  p.  191,  pi.  31,  figs. 


1-1  a.  Middle  Cambrian. 

Bathyurellus  Billings,  1865;  Pal.  Foss.,  vol.  1,  p.  262. 

abruptus  Billings,  1865  ; Pal.  Foss.,  vol.  1,  p.  263,  fig.  247.  Quebec. 

[ Asaphiscus]  hradleyi  Meek.  (See  Asaphiscus  bradleyi.) 

expansus  Billings,  1865  ; Pal.  Foss.,  vol.  1,  p.  318,  figs.  306  a,  b.  Quebec. 

Compare  B.  nitidus  and  B.  marginatus  Billings. 

formosus  Billings,  1865;  Pal.  Foss.,  vol.  1,  p.265,  fig.  250.  Quebec. 

fraternus  Billings,  1865;  Pal.  Foss.,  vol.  1,  p.  267,  fig.  251.  Quebec. 

The  head  of  this  species  may  belong  to  Salter’s  genus  Siygina. 

litoreus  Billings,  1865;  Pal.  Foss.,  vol.  1,  p.  320.  Quebec. 

marginatus  Billings,  1865;  Pal.  Foss.,  vol.  1,  p.  263,  fig.  248.  Quebec. 

Compare  B.  nitidus  and  B.  expansus  Billings. 

nitidus  Billings,  1865;  Pal.  Foss.,  vol.  1,  p.  265,  fig.  249.  Quebec. 


On  page  320  Mr.  Billings  says  that  it  may  be  found  necessary  to  unite  B. 
nitidus,  B.  marginatus,  and  B.  expansus  into  one  polymorphic  species. 


VOGDES  1 


CATALOGUE  OF  TRILOBITES. 


97 


Bathyurellus  rarus  Billings,  1865;  Pal.  Foss., 'vol.  1,  p.  320,  no  lignre.  Quebec. 
— — [ Dikelocephalus ] truncatus  Meek,  1873;  6tli  Ann.  Rept.  Geol.  Survey  Terri- 
tories, p.  465  (no  description  given). 

validus  Billings,  1865 ; Pal.  Foss.,  vol.  1,  p.  268,  fig.  252.  Quebec. 

[ Asaphiscus ] wheeleri.  (See  Asaphiscus  wheeleri.) 

Bathyuriscus  Meek,  1873;  6th  Ann.  Rept.  U.  S.  Geol.  Survey  Territories,  p.  484. 

[Bathyiirusf]  haydeni  Meek,  1873;  6th  Ann.  Rept.  U.  S.  Geol.  Survey  Terri- 
tories, p.  483.  Potsdam. 

haydeni  Walcott,  1886 ; Bull.  U.  S.  Geol.  Survey,  No.  30,  p.  215. 

howelli  Walcott,  1886 ; Bull.  U.  S.  Geol.  Survey,  No.  30,  p.  216,  pi.  30,  figs.  2, 2 a. 

Middle  Cambrian. 

Syn.,  Emholimus  rotundatus  (Rominger)  Walcott,  1888;  Am.  Jour.  Sci.,  3d  series, 
vol.  36,  p.  165,  referred  to  Bathyuriscus  howelli. 

LOgygia~\  producta  Hall  and  Whitfield,  1877 ; U.  S.  Geol.  Expl.  40th  Par.,  vol. 

4,  p.  244,  pi.  2,  figs.  31-34.  Middle  Cambrian. 

VOgyyia']  producta  Hall  and  Whitfield,  1877;  U.  S.  Geol.  Expl.  40th  Par.,  vol. 

4,  p.  245,  pi.  2,  fig.  35. 

producta  Walcott,  1886 ; Bull.  U.  S.  Geol.  Survey,  No.  30,  p.  217,  pi.  30,  figs.  1, 

1 a-c. 

Bathyurus  Billings,  1859  ; Canadian  Naturalist,  vol.  4,  p.  364. 

Type,  Bathyurus  extans  Hall. 

amplimarginatus  Billings,  1857 ; Canadian  Naturalist,  vol.  4,  p.  365,  fig.  12  a,  b. 

Calciferous. 

amplimarginatus  Billings,  1863 ; Geol.  Canada,  p.  122,  fig.  41. 

amplimarginatus  Billings,  1865;  Pal.  Foss.,  vol.  1,  p.  352,  fig.  341  a. 

angelini  Billings,  1859 ; Canadian  Naturalist,  vol.  4,  p.  467,  fig.  37.  Chazy. 

angelini  Billings,  1863 ; Geol.  Canada,  p.  133,  fig.  68. 

arcuatus  Billings,  1865;  Pal.  Foss.,  vol.  1,  p.  205,  fig.  190.  Quebec. 

armatus  Billings,  1860  ; Canadian  Naturalist,  vol.  5,  p.  319,  fig.  23. 

armatus  Billings,  1865  ; Pal.  Foss.,  vol.  1,  p.  411,  fig.  392. 

armatus  Walcott,  1879  ; 32d  Rept.  New  York  State  Mus.  Nat.  Hist.,  p.  131. 

[ Dorypyge? ] armatus  Vogdes,  Bull.  U.  S.  Geol.  Survey  No.  63  (this  bulletin). 

bitub erculatus  Billings,  1860;  Canadian  Naturalist,  vol.  5,  p.  319,  fig.  22;  also 

Geol.  Canada,  1863,  p.  238,  fig.  270.  Quebec. 

bituberculatus  Billings,  1865;  Pal.  Foss.,  vol.  1,  p.  410,  fig.  391. 

If  this  species  is  correctly  represented  by  Mr.  E.  Billings  it  can  not  bo  in- 
cluded within  the  limits  of  Bathyurus.  As  we  know  of  no  other,  to  which  it 
bears  a resemblance,  the  new  generic  term  of  Lloydia  is  proposed,  in  honor  of 
the  first  author  on  Trilobites,  Edward  Lliwyd.  Diagnosis : Glabella  tumid 
and  extending  to  the  frontal  limb  ; basal  lobes  elongate-oval,  pointed  at  both 
ends,  separated  from  the  glabella  by  shallow,  obscure  grooves ; eyes  opposite 
the  mid  length  of  the  glabella  ; thorax  unknown. 

breviceps  Billings,  1865;  Pal.  Foss.,  vol.  1,  p.  262,  fig.  246.  Quebec. 

capax  Billings,  1860;  Canadian  Naturalist,  vol.  5,  p.  318,  fig.  20.  Quebec. 

capax  Billings,  1863;  Geol.  Canada,  p.  238,  fig.  271. 

capax  Billings,  1865;  Pal.  Foss.,  vol.  1,  p.  409,  fig.  389. 

A similar  species  was  referred  by  Mr.  R.  P.  Whitfield  (Geol.  Survey  Wiscon- 
sin, vol.  4,  pi.  4,  fig.  6)  to  Dicelloccphalus. 

caudatus  Billings,  1865;  Pal.  Foss.,  vol.  1,  p.  261,  fig.  245.  Quebec. 

conicua  Billiugs,  1859;  Canadian  Naturalist,  vol.  4,  p.  366,  fig.  12  d.  Calciferous. 

conicua  Billings,  1863;  Geol.  Canada,  p.  122,  fig.  42. 

conicua  Billings,  1865  ; Pal.  Foss.,  vol.  1,  p.  352,  fig.  341  b. 

conicua  Whitfield,  1889  ; Bull.  Am.  Mus.  Nat.  Hist.,  vol.  2,  No.  2,  p.  61,  pi.  13, 

figs.  15-21. 


Bull.  63 7 


98 


A BIBLIOGRAPHY  OF  PALEOZOIC  CRUSTACEA. 


[BULL.  63. 


Bathyurus  ? congeneris  Walcott,  1884;  Pal.  Eureka  Dist.,  Mon.  U.  S.  Geol.  Survey, 
vol.  8,  p.  92,  pi.  12,  fig.  8.  Pogonip. 

cordai  Billings,  1860  ; Canadian  Naturalist,  vol.  5,  p.  321,  fig.  26.  Calciferous. 

cordai  Billings,  1863 ; Geol.  Canada,  p.  238,  fig.  269. 

cordai  Billings,  1865 ; Pal.  Foss.,  vol.  1,  p.  259,  fig.  242;  p.  412,  fig.  395. 

Compare  this  species  with  typical  Solenopleura. 

? crotalifrons  Dwight,  1884;  Am.  Jour.  Sci.,  3d  series,  vol.  27,  p.  253,  figs.  4, 

4 a,  5,  6.  Calciferous. 

cybele  Billings,  1859 ; Canadian  Naturalist,  vol.  4,  p.  366,  fig.  12  c.  Calciferous. 

cybele  Billings,  1863 ; Geol.  Canada,  p.  122,  fig.  43. 

cybele  Billings,  1865;  Pal.  Foss.,  vol.  1,  p.  352,  fig.  341c. 

dubius  Billings,  1860  ; Canadian  Naturalist,  vol.  5,  p.  319,  fig.  21.  Quebec. 

dubius  Billings,  1865;  Pal.  Foss.,  vol.  1,  p.  410,  fig.  390. 

[ Asaphus? ] extans  Hall,  1847;  Pal.  New  York,  vol.  1,  p.  228,  pi.  60,  figs.  2a-c. 

Trenton. 

[ Asaphus  f ] extans  Hall,  1850 ; 3d  Rept.  New  York  State  Cab.  Nat.  Hist.,  p.  174, 

pi.  3,  figs.  1 a-c. 

Syn.,  Asaphus  nodosiriatus  Hall,  1850  ; 3d  Rept.  New  York  State  Cab.  Nat.  Hist., 
p.  175. 

extans  Billings,  1863;  Geol.  Canada,  p.  153,  fig.  114. 

gregarius  Billings,  1865 ; Pal.  Foss.,  vol.  1,  p.  363,  fig.  349.  Potsdam. 

Mr.  Walcott  (Bull.  U.  S.  Geol.  Survey,  No.  10,  p.  36)  refers  this  species  to 
the  genus  Solenopleura  Angelin,  and  remarks  that  many  of  the  Cambrian  species 
of  the  genus  Bathy  urus  described  in  the  Canadian  reports  might  be  referred  to 
that  genus? 

? haydeni.  (See  Bathyuriscus  haydeni.) 

longispinus  Walcott,  1876  ; 28th  Rept.  N.  Y.  State  Cab.  Nat.  Hist.,  p.  94. 

Trenton. 

minganensis  Billings,  1865 ; Pal.  Foss.,  vol.  1,  p.  353.  Calciferous. 

nero.  (See  Solenopleura  nero  (Billings)  Walcott.) 

oblongus  Billings,  1860  ; Canadian  Naturalist,  vol.  5,  p.  321,  fig.  25.  Quebec. 

oblongus  Billings,  1865;  Pal.  Foss.,  vol.  1,  p.  412,  fig.  394. 

parvulus  Billings,  1861;  Geol.  Vermont,  vol.  2,  p.  952,  fig.  361. 

parvulus  Billings,  1861 ; Pal.  Foss.,  Bull.  Geol.  Sur.  Canada  p.  16,  fig.  21. 

Potsdam. 

parvulus  Billings,  1865 ; Pal.  Foss.,  vol.  1,  p.  16,  fig.  21. 

perplexus  Billings,  1865;  Pal.  Foss.,  vol.  1,  p.  364,  fig.  350.  Potsdam. 

perspicator  Billings,  1865;  Pal.  Foss.,  vol.  1,  p.  205,  fig.  191.  Quebec. 

pogonipensis  Hall  and  Whitfield,  1877;  U.  S.  Geol.  Expl.  40th  Par.,  vol.  4,  p. 

243,  pi.  1,  figs.  33, 34.  Cambrian. 

quadratus  Billings,  1860;  Canadian  Naturalist,  vol.  5,  p.  321,  fig.  27.  Quebec. 

quadratus  Billings,  1865 ; Pal.  Foss.,  vol.  1,  p.  412,  fig.  396. 

saffordi  Billings,  1860  ; Canadian  Naturalist,  vol.  5,  p.  321,  fig.  24.  Quebec. 

saffordi  Billings,  1865 ; Pal.  Foss.,  vol.  1,  p.  259,  fig.  341 ; p.  411,  fig.  393. 

seelyi  Whitfield,  1886 ; Bull.  Am.  Mus.  Nat.  Hist.,  New  York,  vol.  1,  No.  8,  p.  339, 

pi.  33,  figs.  12-18.  Birdseye. 

seelyi  Whitfield,  1889 ; Bull.  Am.  Mus.  Nat.  Hist. , New  York,  vol.  2,  No.  2,  p.  62, 

pi.  13,  figs.  8-14. 

senectus  Billings,  1861 ; Bull.  Geol.  Sur.  Canada,  p.  16.  Potsdam. 

senectus  Billings,  1861 ; Geol.  Vermont,  vol.  2,  p.  953,  figs.  359, 360. 

senectus  Billings,  1863 ; Geol.  Canada,  p.  286,  figs.  298  a,  b ; Pal.  Foss.,  vol.  1.  p. 

16  (1865),  figs.  19,20. 

Referred  to  Protypus  senectus  Walcott,  1886 ; Bull.  U.  S.  Geol.  Survey,  No.  30, 
p.  213,  pi.  31,  figs.  2,  2 a-c. 


VOGDBS.  ] 


CATALOGUE  OF  TRILOBITES. 


99 


Bathyurus  serratus  Meek,  1873;  6th  Ann.  Kept.  U.  S.  Geol.  Survey  Territories,  p. 
480.  Potsdam. 

? simillimus  Walcott,  1884 ; Pal.  Eureka  Dist.,  Mon.  U.  S.  Geol.  Survey,  vol.  8,  p. 

93,  pi.  12,  fig.  11.  Pogonip. 

smithi  Billings,  1863;  Geol.  Canada,  p.  153,  fig.  115.  Trenton. 

smithi  Billings,  1865 ; Pal.  Foss.,  vol.  1,  p.  56. 

solitaricus  Billings,  1865  ; Pal.  Foss.,  vol.  I,j9.  362.  Quebec. 

[^cidaspis]  spiniger  Hall,  1847  ; Pal.  New  York,  vol.  1,  p.  241,  pi.  64,  fig.  5. 

Trenton. 

stonemani  Yogdes,  1884  ; 12th  Ann.  Kept.  Geol.  Nat.  Hist.  Minnesota,  p.  8. 

Trenton. 

strenuus  Billings,  1865;  Pal.  Foss.,  vol.  1,  p.204,  fig.  188.  Quebec. 

taurifrons  Dwight,  1884  ; Am.  Jour.  Sci.,  3d  series,  vol.  27,  p.  252,  pi.  7,  figs.  1-3. 

Calciferous. 

timon  Billings,  1865 ; Pal.  Foss.,  vol.  1,  p.  261,  fig.  244.  Quebec. 

? tuberculatus  Walcott,  1884  ; Pal.  Eureka  Diet.,  Mon.  U.  S.  Geol.  Survey,  vol. 

8,  p.  12,  fig.  9.  Pogonip. 

vetula  Billings,  1865;  PaT.  Foss.,  vol.  1,  p.  365.  ^ Potsdam. 

[ Agraulos  ( Batliym'us?) ] woosteri  Whitfield,  1878;  Ann.  Rept.  Geol.  Survey 

Wisconsin,  p.  56.  Potsdam. 

[ Agraulos  {Bathyurus  ?)]  woosteri  Whitfield,  1882;  Geol.  Wisconsin,  vol.  4,  p. 

189,  pi.  1,  figs.  19-21. 

Bohemilla  Batrande,  1872;  Syst.  Sil.  Boheme,  Suppl.,  vol.  1,  p.  137. 

Type,  Bohemilla  stupenda  Barrande. 

Brongniartia  Eaton,  Am.  Jour.  Sci.,  1st  series,  vol.  22,  p.  166,  and  Geol.  Text-Book,  p. 
32  (Syn.,  Asaphus  in  part),  not  Brongniartia  Salter  (subgenus  Homalonotus). 

carcinoides  Eaton.  (See  Triarthrus  becki.) 

isoletea.  (See  Asaphus  platycephalus.) 

platycephus  Eaton.  (See  Homalonotus  delphinocephalus.) 

Brachymetopus  McCoy,  1847;  Ann.  Nat.  Hist.,  vol.  20,  p.  220. 

Type,  Brachymetopus  maccoyi  Portlock. 

\_Phillip8ia  ( Griffithides )]  lodiensis  Meek,  1875;  Pal.  Ohio,  vol.  2,  p.  323,  pi.  18, 

fig.  3.  Waverly. 

lodiensis  Yogdes,  1888;  Annals  New  York  Acad.  Sci.,  vol.  4,  p.  102. 

[ Phillipsia  ( Brachymetopus )]  ornata  Hall.  (See  Cyphaspis  ornata.) 

Bronteus  Goldfuss,  1839;  feeitrage  Petrefactenkunde,  Nova  Acta  Physico-Med.,  vol. 
19,  p.  360,  pi.  33,  fig.  3. 

Type,  Bronteus  flahellif era  Goldfuss. 

Syn.,  Goldius  De  Koninck,  1841 ; M6m.  Crust.  Foss.  Belgique,  p.  5. 

acamas  Hall,  1865;  20th  Rept.  New  York  State  Cab.  Nat.  Hist.,  p.  332,  pi.  21, 

figs.  19,20.  Niagara. 

acamas  Hall,  1870;  20th  Rept.  New  York  State  Cab.  Nat.  Hist.,  p.  422,  pi.  21, 

figs.  19, 20  (rev.  ed.). 

barrandi  Hall,  1859;  Pal.  New  York,  vol.  3,  p.  350,  pi.  63,  figs.  1-4. 

Lower  Helderberg. 

canadensis  Logan,  1844;  Geol.  Canada,  p.  54, 2 figs.  Lower  Helderberg. 

insularis  Billings,  I860;  Catalogue  Sil.  Foss.  Anticosti,  p.  66. 

laphami  Whitfield,  1878;  Ann.  Rept.  Geol.  Survey  Wisconsin  (1877),  p.  88. 

Niagara. 

laphami  Whitfield,  1882  ; Geol.  Wisconsin,  vol.  4,  p.  310,  pi.  22,  figs.  1-4. 

lunatus  Billings,  1857;  Geol.  Canada,  p.  338.  Trenton. 

lunatus  Billings,  1863;  Geol.  Canada,  p.  188,  fig.  187. 

? niagarensis  Hall,  1852;  Pal.  Now  York,  vol.  3,  p.  314,  pi.  70,  fig.  3. 


Niagara. 


100 


A BIBLIOGRAPHY  OF  PALEOZOIC  CRUSTACEA, 


[BULL.  63. 


Bronteus  occasus  Winehell  and  Marey,  1866;  Mem.  Boston  Soc.  Nat.  Hist.,  vol.  1, 
p.  104,  pi.  3,  fig.  12.  Niagara. 

occasus  (Winehell  and  Marey)  Hall,  1867  ; 20th  Rept.  New  York  State  Cab.  Nat. 

Hist.,  p.  400. 

pompilius  Billings,  1863;  Proc.  Portland  Soc.  Nat.  Hist.,  p.  123,  pi.  1,  fig.  25. 

Upper  Silurian. 

tullius  Hall,  1888;  Pal.  New  York,  vol.  7,  p.  12,  pi.  8,  figs.  34-36.  Hamilton. 

Bumastus  Murchison,  1839 ; Sil.  Syst.,  p.  656.  Subgenus,  Illcenus. 

Calymene  Brongniart,  1822 ; Crust.  Fos.,  p.  9. 

Type,  Calymene  tuberculata  Biinnich,  1781. 

Syn.,  Prionocheilus,  Rouault,  Bull.  Soc.  G6ol.  France,  vol.  4,  1846,  p.  309. 

anchiops.  (See  Dalmanites  anchiops.) 

beckii.  (See  Triarthrus  becki.) 

blumenbachi  Brongniart,  1822;  Crust.  Foss.,  p.  11,  pi.  1,  figs.  1 a-d. 

■ blumenbachi  Barrande,  1852;  Syst.  Sil.  Boherne,  pis.  19  and  45. 

blumenbachi  Salter,  1863;  Mon.  Brit.  Trilobites,  pi.  8,  figs.  7-11,  13-16;  pi.  9, 

fig.  1. 

This  species  should  take  the  older  name  of  Calymene  tuberculata  Biinnich. 

blumenbachi  (Green)  not  Brong.,  Mon.  Tril.  N.  A.,  p.  28,  cast  1. 

blumenbachi  ? Foerste,  1885 ; Bull.  Denison  Univ.,  vol.  1,  p.  100,  pi.  13,  fig.  25. 

bucklandi.  (See  Ceraurus  pleurexanthus  Green.) 

bufo.  (See  Fhacops  bufo  Green.) 

bufo  var.  rana.  (See  Phacops  rana  Green.) 

callicephala  Green,  1832;  Mon.  Tril.  N.  A.,  p.  30,  cast  2. 

callicephala'Burmeister,  1843 ; Org.  Trilobiten,  p.  83,  pi.  2,  figs.  9-10  (Ray  Soc. 

ed.). 

callicephala  Miller,  1882 ; Jour.  Cincinnati  Soc.  Nat.  Hist.,  vol.  5,  p.  117,  pi.  5, 

fig.  8. 

The  cast  of  this  species  (from  a dark  yellowish  limestone  of  Hampshire 
County,  Virginia),  issued  with  Dr.  Green’s  monograph,  exhibits  a Calymene 
with  a broad  frontal  margin.  The  other  specimens  referred  to  by  Dr.  Green 
from  Ohio  and  Indiana  are  species  of  the  well-known  Calymene  senaria  Conrad. 

camerata  Conrad,  1842;  Jour.  Acad.  Nat.  Sci.  Phila.,  vol.  8,  p.  278.  Niagara. 

camerata  Hall,  1852;  Pal.  New  York,  vol.  2,  p.  337,  pi.  78,  figs.  10  a-f. 

christyi  Hall,  1860;  13th  Rept.  New  York  State  Cab.  Nat.  Hist.,  p.  119. 

Hudson. 

christyi  Hall,  1862;  15th  Rept.  New  York  State  Cab.  Nat.  Hist.,  pi.  10,  figs.  1,2, 

and  5. 

• christyi  Hall  and  Whitfield,  1875 ; Pal.  Ohio,  vol.  2,  p.  107,  pi.  4,  figs.  13-15. 

christyi  Miller,  1874 ; Cincinnati  Quart.  Jour.  Sci.,  vol.  1,  p.  141. 

[ Hemicrypturis ] clintoni  Vanuxem,  1842;  Geol.  New  York,  3d  Geol.  Dist.,  p.  79, 

fig.  3;  also  p.  80.  Clinton. 

clintoni  Hall,  1852;  Pal.  New  York,  vol.  2,  p.  298,  pi.  66  a,  figs.  5 a-d. 

clintoni  Rogers,  1858  ; Geol.  Survey  Pennsylvania,  vol.  2,  p.  823,  fig.  637. 

clintoni  Vogdes,  1880;  Proc.  Acad.  Nat.  Sci.  Phila.,  p.  178,  figs.  3,4  (not  fig.  3). 

clintoni  Vogdes,  1886;  Des.  New  Species  Foss.  Crust.  Clinton  Group,  p.  5,  figs.  3, 4. 

(See  Calymene  vogdesii  Foerste.) 

conradi  Emmons,  1855;  Am.  Geology,  vol.  1,  pt.  2,  p.  236.  Hudson. 

crassimarginata.  (See  Proetus  crassimarginata.) 

diops  Green,  1832 ; Mon.  Tril.  N.  A.,  p.  37,  pi.  1,  fig.  2,  cast  8 ( Proetus  diops).  • 

macrophthalma  Green,  1832 ; Mon.  Tril.  N.  A.,  p.  39,  cast  9.  (See  Phacops  bufo. ) 

mamillata  Hall,  1861 ; Geol.  Wisconsin,  p.  50.  Trenton. 

mamillata  Hall,  1862;  Geol.  Wisconsin,  vol.  1,  p.  432,  figs.  1,2. 

marginatus.  (See  Proetus  marginatus.) 


V0GDE8. 1 


CATALOGUE  OF  TRILOBITES. 


101 


Calymene  microps  Green,  1832;  Mon.  Tr.il.  N.  A.,  p.  34,  cast  6. 

multicosta  Hall,  1847 ; Pal.  New  York,  vol.  l,p.  228,  pi.  60,  fig.  3.  Trenton. 

nasuta  Ulrich,  1879;  Jour.  Cincinnati  Soc.  Nat.  Hist.,  vol.  2,  p.  131,  fig.  3. 

Niagara. 

niagarensis  Hall,  1843;  Geol.  New  York,  4th  Dist.,  p.  102,  fig.  3 (on  p.  101). 

Niagara. 

blumenbachii  var.  niagarensis  Hall,  1852 ; Pal.  New  York,  vol.  2,  p.  307,  pi.  67, 

figs.  11, 12. 

blumenbachii  Roemer,  1860;  Sil.  Fauna  W.  Tenn.,  p.  79,  pi.  5,  fig.  22. 

niagarensis  Hall  and  Whitfield,  1875 ; Pal.  Ohio,  vol.  2,  p.  153,  pi.  7,  figs.  14, 15. 

niagarensis  Hall;  20th  Rept.  New  York  State  Cab.  Nat.  Hist.,  p.  334  ; revised 

edition,  p.  425. 

niagarensis  Hall,  1876;  Illus.  Devon.  Foss.  Crustacea,  pi.  1,  fig.  10. 

niagarensis  Hall,  1879 ; 28th  Rept.  N.  Y.  State  Mus.  Nat.  Hist.,  p.  187,  pi. 32,  figs. 

8-15. 

niagarensis  Hall,  1883;  11th  Ann.  Rept.  Geol.  Nat.  Hist.  Indiana,  1881,  p.  331. 

pi.  34,  figs.  8-15. 

Compare  C.  brevicapitata  (Portlock)  McCoy;  Brit.  Pal.  Foss.,  pi.  1 F, fig. 4. 

nupera.  (See  Phacops  nupera.) 

odontocephala.  (Syn.,  Dalmanites  selenus.) 

phlyctainodes  Green,  1837 ; Am.  Jour.  Sci.,  1st  series,  vol.  32,  p.  167. 

Dr.  Green  compares  this  species  with  Encrinurus  variolaris. 

platys  Green,  1832;  Mon.  Tril.  N.  A.,  p.  32,  casts  4,5.  Upper  Helderberg. 

platys  Hall,  1861 ; Des.  New  Species  Foss.,  p.  54. 

platys  Hall,  1862;  15th  Rept.  New  York  State  Cab.  Nat.  Hist.,  p.  82. 

platys  Hall,  1876 ; Illus.  Devon.  Foss.  Crustacea,  pi.  1,  figs.  1-9. 

platys  Hall,  1888;  Pal.  New  York,  vol.  7,  p.  1,  pi.  1,  figs.  1-9;  pi.  25,  figs. 

1,2. 

rana.  (See  Phacops  rana  Green.) 

rostrata  Yogdes,  1879;  Am.  Jour.  Sci.,  3d  series,  vol.  18,  p.  477.  . Clinton. 

rostrata  Vogdes,  1880;  Proc.  Acad.  Nat.  Sci.  Phila.,  p.  176,  figs.  1,2. 

rostrata  Yogdes,  1886;  Des.  New  Species  Foss.  Crust.  Clinton  Group,  p.  2,  figs. 

1,2. 

rowi.  (See  Phacops  rowi  Green.) 

- — rugosa  Shumard,  1855;  1st  and  2d  Repts.  Geol.  Missouri,  p.  200,  pi.  B,  fig.  14. 

Lower  Helderberg. 

selenecephala.  (See  Calymene  senaria  Conrad.) 

senaria  Conrad,  1841;  4th  Ann.  Rept.  Pal.  Dept.  New  York  Geol.  Survey,  p.  49. 

Trenton. 

senaria  Emmons,  1842;  Geol.  New  York,  2d  Geol.  Dist.,  p.  390,  fig.  2. 

Syn.,  selenecephala  Green,  1832  ; Mon.  Tril.  N.  A.,  p.  31,  cast  3. 

blumenbachii  Green,  1832;  Mon.  Tril.  N.  A.,  p.  28,  cast  1.  (Not  of  Bron- 
gniart.) 

callicephala  Green,  1832;  Mon.  Tril.  N.  A.,  p.  31.  (Specimens  from  Ohio 
and  Indiana  only.) 

brevicapitata  Salter,  1848 ; Mem.  Geol.  Surv.  United  Kingdom,  vol.  2,  p.  341, 
pi.  11,  figs.  1,  2.  (Not  of  Portlock,  1843  ; Geol.  Rept.  Londonderry,  etc., 
p.  286,  pi.  3;  fig.  3.) 

brevicapitata  (Portlock)  Salter;  Mem.  Geol.  Surv.  United  Kingdom,  vol.  3, 
pi.  17,  figs.  11,  12.  (Not  of  Portlock.) 
forcipata  (McCoy)  Salter;  Palaeon.  Soc.  London,  vol.  17,  p.  97.  (Not  of 
McCoy,  Sil.  Foss.  Ireland,  pi.  4,  fig.  14.) 

senaria  Emmons,  1855;  Am.  Geology,  vol.  1,  pt.  2,  p.  213,  pi.  16,  fig.  9. 

senaria  Hall,  1847 ; Pal.  New  York,  vol.  1,  p.  238,  pi.  64,  figs.  3 a-n. 


[BULL.  63. 


102  A BIBLIOGRAPHY  OF  PALEOZOIC  CRUSTACEA. 

Calymene  \bhinienbachii]  var.  senaria  Hall,  1852;  Pal.  New  York,  vol.  2,  p.  290,  pi. 
66  a,  tigs.  6 a-e.  Clinton. 

senaria  var.  blumenbachii  Salter,  1865;  Mon.  Brit.  Tril.,  p.  97,  pi.  9,  figs.  6-10  (not 

figs.  7, 8,  Calymene  brevicapitata  Portlock). 

senaria  Meek,  Pal.  Ohio,  vol.  1,  p.  173,  pi.  14,  figs.  14  a-f. 

senaria  Miller,  1874;  Cincinnati  Quart.  Jour.  Sci.,  vol.  1,  p.  140. 

Syn.,  calhcephala  (Green)  Miller,  1877 ; Catalogue  Am.  Pal.  Foss.,  p.  213. 

senaria  White,  1880;  2d  Ann.  Rept.  Dept.  Statistics  Geol.  Indiana,  p.  493,  pi.  2, 

figs.  1,2. 

Syn.,  callicephala  (Green)  Miller,  1882;  Jour.  Cincinnati  Soc.  Nat.  Hist.,  vol.  5, 
p.  117,  pi.  5,  fig.  8. 

senaria  Walcott,  1887 ; Notes  on  Some  Sections  of  Trilobites,  pi.  1. 

senaria  Walcott,  1884  ; Science,  March  7, 1884,  vol.  3,  p.  201,  figs.  2, 3. 

spinifera  Conrad,  1842;  Jour.  Acad.  Nat.  Sci.  Phila.,  vol.  8,  p.  277. 

Compare  Cyphaspis  girardeauensis. 

trisulcata.  (See  Phacops  trisulcata.) 

vogdesii  Foerste,  1887;  Bull.  Denison  Univ.,  vol.  2,  p.  95,  pi.  8,  figs.  12-16. 

Clinton. 

? blumenbachi  Foerste,  1886 ; Bull.  Denison  Univ.,  vol.  1,  p.  190,  pi.  13,  fig.  24. 

Syn.,  clintoni  Yogdes,  1882  ; Proc.  Acad.  Nat.  Sci.  Phila.,  p.  178,  fig.  3 (not  fig.  4). 
clintoni  Yogdes,  1886;  Des.  New  Species  Foss.  Crust.  Clinton  Group,  p.  5, 
fig.  3 (not  fig.  4). 

Ceratocephala  Warder,  1838.  (See  Acidaspis.) 

ceralepta  Anthony.  (See  Acidaspis  ceralepta.) 

goniata  Warder,  1838;  Am.  Jour.  Sc.,  1st  series,  vol.  34,  p.  378,  figure. 

Ceratolichas  Hall,  1888  ; Pal.  New  York,  vol.  7,  p.  xl.  Subgenus  Lichas. 

Ceraurus  Green,  1832;  Monthly  Am.  Jour.  Geol.,  vol.  1,  p.  560,  pi.,  fig.  6;  Mon.  Tril. 

N.  A.,  p.  83,  cast  33,  pi.,  fig.  10. 

Ceraurus  Hall,  1847;  Pal.  New  York,  vol.  1,  p.  242. 

Syn.,  Otarion  (in  part)  Zenker,  1833 ; Beitrage  Nat.  Urwelt,  p.  44. 

Arges  (in  part)  Goldfuss,  1843;  Neues  Jahrbuch  fur  Mineral.,  p.  5. 
Cyphaspis  (in  part)  Burmeister,  1843,  Org.  Trilobiten,  p.  104. 

Amphion  (in  part)  Portlock,  1843;  Geol.  Survey  Londonderry,  etc.,  p.  272. 
Cyphaspis  (in  part)  McCoy,  1846 ; Sil.  Foss.  Ireland,  p.  44. 

Cheirurus  Beyrich,  1846 ; Unters.  Trilobiten,  etc.  II,  p.  3. 

Eccoptochile  Corda,  1847 ; Prodr.,  p.  245. 

Actinopeltes  Corda,  1847 ; Prodr.,  p.  247. 

Crotalocephalus  Salter,  1853 ; Mem.  Geol.  Survey  United  Kingdom,  decade 
7,  pi.  2,  p.  10. 

Cyrtometopus  Angelin,  1854;  Pal.  Scand.,  p.  32. 

Sphcerocoryphe  Angelin,  1854;  Pal.  Scand.,  p.  65. 

Pseudophceroxochus  Schmidt,  1881;  Rev.  Baltic  Sil.  Tril.,  p.  130. 
Nieszkowskia  Schmidt,  1881 ; Rev.  Baltic  Sil.  Tril.,  p.  130. 

Type,  Ceraurus  pleurexanthemus  Green. 

ICheirurus ] appollo  Billings,  1860;  Canadian  Naturalist,  vol.  5,  p.  322,  fig.  28. 

Quebec. 

[Cheirurus']  appollo  Billings,  1865;  Pal.  Foss.,  vol.  1,  p.  413,  fig.  397. 

[Cheirurus ] bimucronatus  (Murch.)  Roemer,  Die  sil.  Fauna  W.  Tenn.,  p.  80,  pi.  5, 

fig.  19,  not  of  Murchison.  (See  Ceraurus  niagarensis  Hall.) 

crosotus  Lock.  (See  Acidaspis  crosotus.) 

[Cheirurus]  eryx  Billiugs,  1860 ; Canadian  Naturalist,  vol.  5,  p.  322,  fig.  30. 

Quebec. 

[Cheirurus]  eryx  Billings,  1865;  Pal.  Foss.,  vol.  1,  p.  413,  fig.  399. 

[Cheirurus]  glaucus  Billings,  1865 ; Pal.  Foss.,  vol.  1,  p.  323,  fig.  308.  Quebec. 


VODGES.] 


CATALOGUE  OF  TRILOBITES. 


103 


Ceranrus  [Cheirurus}  icarus  Billings,  1860 ; Canadian  Naturalist,  vol.  5,  p.  67,  fig.  14. 

Hudson. 

[Cheirurus}  icarus  Billings,  1863;  Geol.  Canada,  p.  219,  fig.  231. 

icarus  Meek,  1873 ; Pal.  Ohio,  vol.  1,  p.  162,  pi.  14,  fig.  11  a,  b,  c. 

icarus  Miller,  1874;  Cincinnati  Quart.  Jour.  Sci.,vol.  l,p.  133. 

[Cheirurus}  insignis  (Beyrich)  Hall,  1852;  Pal.  New  York,  vol.  2,  p.  300,  also 

p.  306,  pi.  67,  figs.  9, 10. 

Not  of  Beyrich,  1845;  Ueber  einige  bohm.  Tril.,  p.  12,  pi.  1,  fig.  1, 

insignis.  (See  Ceraurus  niagarensis  Hall.) 

mercurius  Billings,  1865;  Pal.  Foss.,  vol.  1,  p.  285,  fig.  272.  Quebec. 

niagarensis  Hall,  1867  ; 20tb  Kept.  New  York  Stale  Cab.  Nat.  Hist.,  p.  376,  pi. 

21,  fig.  10. 

niagarensis  Hall,  1870;  20th  Rept.  New  York  State  Cab.  Nat.  Hist.  (2d  ed.),  p. 

427,  pi.  21,  figs.  10,  11. 

Syn.,  Sphcerexochus  romingeri  ? Hall ; Doc.  Ed.  2Sfch  Rept.  New  York  State  Mus. 
Nat.  Hist. 

Explanation  of  pi.  32,  fig.  16  (erroneous  reference). 

[ Cheirurus ] niagarensis  Hall,  1879 ; 28th  Rept.  New  York  State  Mus.  Nat.  Hist., 

p.  189,  pi.  32,  fig.  16. 

Syn.,  Cheirurus  bimucronatus  (Murch.)  Roerner ; Die  sil.  Fauna  W.  Tenn.,  p.  80, 
pi.  5,  fig.  19. 

niagarensis  Hall,  1882;  12th  Ann.  Rept.  Geol.  Nat.  Hist.  Indiaua,  1881,  p.  335, 

pi.  34,  fig.  16;  pi.  33,  fig.  10. 

[Cheirurus}  numitor  Billings,  1866  ; Catalogue  Sil.  Foss.  Anticosti,  p.  27,  fig.  11. 

Hudson. 

[ Cheirurus ] nuperus  Billings,  1866;  Catalogue  Sil.  Foss.  Anticosti,  p.  61,  fig.  20. 

Anticosti. 

[Cheirurus}  perforator  Billings,  1865;  Pal.  Foss.,  vol.  1,  p.  287,  fig.  275. 

Quebec. 

pleurexanthemus  Green,  1832;  Monthly  Am.  Jour.  Geol.,  vol.  1,  p.  560,  pi., 

fig.  10.  Trenton  and  Hudson. 

pleurexanthemus  Green,  1832;  Mon.  Tril.  N.  A.,  p.  84,  fig.  10,  pi.  1,  cast  33. 

Syn.,  Calymene  bucklandi  Anthony,  1838;  Am.  Jour.  Sci.,  1st  series,  vol.  36,  p. 
106,  figs.  1, 2. 

pleurexanthemus  Hall,  1847  ; Pal.  New  York,  vol.  1,  p.  242,  pi.  65,  figs.  1 a-n ; 

pi.  66,  figs.  1, 1 h. 

pleurexanthemus  Emmons,  1855  ; Am.  Geology,  vol.  1,  p.  217,  pi.  15,  figs.  1 a-k. 

[ Cheirurus ] pleurexanthemus  Billings,  1863;  Geol.  Canada,  p.  188,  fig.  188. 

pleurexanthemus  Miller,  1874  ; Cincinnati  Quart.  Jour.  Sci.,  vol.  1,  p.  132. 

pleurexanthemus  Walcott,  1875;  Annals  Nat.  Hist.  New  York,  vol.  11,  p.  155, 

pi.  11. 

pleurexanthemus  Walcott,  1881 ; Bull.  Mus.  Comp.  Zool.  Harvard  Coll.,  vol. 

8,  p.  211,  pi.  5,  figs.  1-6. 

[ Cheirurus}  polydorus  Billings,  1865  ; Pal.  Foss.,  vol.  1,  p.  286,  fig.  274.  Quebec. 

[Cheirurus}  pompilius  Billings,  1865  ; Pal.  Foss.,  vol.  1,  p.  181,  fig.  162. 

Chazy  and  Hudson. 

[ Cheirurus}  prolificus  Billings,  1865  ; Pal.  Foss.,  vol.  1,  p.  285,  fig.  273  ; p.  325,  fig. 

311.  Quebec. 

? pustulosa  Hall,  1847 ; Pal.  New  York,  vol.  1,  p.  246,  pi.  61,  fig.  2 a-li. 

Trenton. 

rarus  Walcott,  1877 ; Advanced  sheets  31st  Rept.  Now  York  State  Mus.  Nat. 

Hist.,  p.  15.  Trenton. 

rarus  Walcott,  1879^  31st  Rept.  New  York  State  Mus.  Nat.  Hist.,  p.  68. 

[Cheirurus}  satyrus  Billings,  1865 ; Pal.  Foss.,  vol.  1 , p.  324,  fig.  309.  Chazy. 


104 


A BIBLIOGRAPHY  OF  PALEOZOIC  CRUSTACEA. 


[BULL.  63. 


Ceraunis  [ Cheirurus ] sol  Billings,  1865 ; Pal.  Foss.,  vol.  1,  p.  288,  fig.  276.  Quebec. 

[ Cheirurus ] solitarius  Billings,  1865 ; Pal.  Foss.,  vol.  1,  p. 206.  . Quebec. 

[ Cheirurus ] tarquinius  Billings,  1863;  Proc.  Portland  Soc.  Nat.  Hist.,  vol.  1,  p. 

121,  pi.  1,  fig.  22.  Upper  Silurian. 

vigilans.  (See  Encrinurus  vigilans.) 

[ Cheirurus ] vulcanus  Billings,  1865;  Pal.  Foss.,  vol.  1,  p.  284,  fig.  27;  p.  324, 

fig.  310.  Quebec. 

Chariocephalus  Hall,  1863 ; 16th  Rept.  New  York  State  Cab.  Nat.  Hist.,  p.  175. 

Type,  Chariocephalus  ivhitjieldi  Hall. 

tumifrons  Hall  and  Whitfield,  1877 ; U.  S.  Geol.  Expl.  40th  Par.,  vol.  4,  p.  224,  pi. 

2,  figs.  38, 39.  Potsdam. 

? tumifrons  Walcott,  1884 ; Pal.  Eureka  Dist.,  Mon.  U.  S.  Geol.  Survey,  vol.  8,  p. 

61,  pi.  10,  fig.  16. 

whitfieldi  Hall,  1863;  16th  Rept.  New  York  State  Cab.  Nat.  Hist.,  p.  175,  pi.  6, 

figs.  49-53 ; pi.  10,  fig.  20.  Potsdam. 

Chasmops  McCoy,  1849;  Annals  Mag.  Nat.  Hist.,  2d  series,  vol.  4,  p.  403.  (See  Dal- 
manites  [ Chasmops ] anchiops,  anchiops  var.  armatus,  anchiops  var.  sobri- 
nus,  D.  [ Chasmops ] calypso,  D.  [Chasmops']  erina,  D.  [ Chasmops ] macrops. 

[ Dahnanites ] troosti  Safford,  1869:  Geol.  Tennessee,  p.  290.  Trenton. 

troosti  Safford  and  Vogdes,  1889;  Proc.  Acad.  Nat.  Sci.  Phila.,  p.  167,  figure. 

Conoceplialus  Zenker,  1833;  Beitrage  Nat.  Urvvelt,  p.  48. 

Conocephalites  Barrande,  1852;  Syst.  Sil.  Boheme,  vol.  1,  p.  415. 

For  species  previously  classed  under  these  genera,  see  Conocoryphe,  Fty- 
choparia,  and  Crepicephalus. 

Conocoryphe  C<irda,  1847  ; Prodr.,  p.  139,  pi.  2,  fig.  10. 

Type,  Conocoryphe  sulzeri  Schlotheim. 

[Conocephalites]  baileyi  Hartt,  1868  ; Acadian  Geology,  p.  645  (3d  ed.).  St.  John. 

baileyi  Matthew,  1884 ; Trans.  Royal  Soc.  Canada,  vol.  1,  p.  Ill,  pi.  1,  figs.  22-27. 

[Bailiella]  baileyi  Matthew,  1884  ; Traus.  Royal  Soc.  Canada,  vol.  1,  pi.  1,  fig.  22. 

[Salteria]  baileyi  Walcott,  1884;  Bull.  U.  S.  Geol.  Survey,  No.  10,  p.  32,  pi.  4, 

figs.  3,  3 a ; pi.  5,  figs.  7,  7 a. 

The  author  herein  proposed  the  subgenus  Salteria  (corrected  to  Bailiella)  for 
Erinnys  Salter,  a preoccupied  generic  name ; the  same  is  true  of  Salteria,  used 
for  a genus  of  fossil  Crustacea. 

[Conocephalites]  calcifera  Walcott,  1879;  32d  Rept.  New  York  State  Mus.  Nat. 

Hist.,  p.  129.  Calciferous. 

[Conocephalites]  cordillerae  Rominger,  1887 ; Proc.  Acad.  Nat.  Sci.  Phila.,  p.  17, 

pi.  1,  fig.  7.  Cambrian. 

elegans  Hartt,  1868;  Acadian  Geol.  (3d  ed.),  p.  650.  St.John. 

elegans  Walcott,  1884;  Bull.  U.  S.  Geol.  Survey,  No.  10,  p.  33,  pi.  4,  figs.  2, 2 a,  b. 

gemini-spinosus  Hartt.  (See  Conocoryphe  matthewi.) 

[Conocephalites]  hartti  Walcott,  1879  ; 32dRept.  New  York  State  Mus.  Nat. Hist., 

p.  131.  Calciferous. 

[Conocephalites]  matthewi  Hartt,  1868;  Acadian  Geology,  p.646,  fig. 224. 

St.  John. 

[Conocephalites]  matthewi  Matthew,  1884;  Trans.  Royal  Soc.  Canada,  vol.  1,  p. 

103,  pi.,  figs.  6-21. 

Syn.,  Harttia  matthewi  Walcott,  1884  ; Bull.  U.  S.  Geol.  Survey,  No.  10,  p.  19,  pi. 
1,  fig.  3. 

matthewi  Walcott,  1884;  Bull.  U.  S.  Geol.  Survey,  No.  10,  p.  28,  pi.  4,  figs.-  1, 

1 a,  b. 

[Conocephalites]  optatus  Hall,  1863;  16th  Rept.  New  York  State  Cab.  Nat.  Hist., 

p.  122,  pi.  5 a,  fig.  7.  * Potsdam. 

[Conocephalites]  trilineatus.  (See  Atops  trilineatus  Emmons.) 


V0GDES.] 


CATALOGUE  OF  TRILOBITES. 


105 


Conocoryphe  [ Conocoryplie ] trilineatus.  (See  Atops  trilineatus  Emmons.) 

— t—  [Bailella J walcotti  Matthew,  1884  ; Trans.  Royal  Soc.  Canada,  vol.  1,  p.  119,  pi. 
1,  figs.  36-36  b.  St.  John. 

walcotti  Walcott,  1884;  Bull.  U.  S.  Geol.  Survey,  No.  10,  p.  30. 

Conolichas  Dames,  1877 ; Zeitschr.  Deutseh.  geol.  Gesell.,  Berlin,  1877,  p.  806.  Cono- 
lichas,  subgenus  Lidias  Hall,  1888;  Pal.  New  York,  vol.  7,  p.  xxxix. 

Coronura  Hall,  1888  ; Pal.  New  York,  vol.  7,  p.  xxxii.  (See  Dalmanties  [ Coronura ] 
aspectans,  D.  [Coronura']  myrmecophorus,  and  D.  [ Coronura ] emargi- 
natus.) 

Corycephalus  Hall,  1888  ; Pal.  New  York,  vol  7,  p.  xxxiv.  (See  Dalmanites  [ Cory - 
eephalus ] regalis,  D.  [Cory  eephalus]  pygmaeus,  and  D.  [Corycephalus]  denta- 
tus.) 

Crepicephalus  Owen,  1852;  Rept.  Geol.  Survey  Wisconsin,  Iowa,  and  Minnesota, 
p.  570. 

There  is  hardly  a question  that  Dr.  D.  D.  Owen  had  before  him  when  he 
wrote  the  description  of  his  genus  Crepicephalus  a true  Ptychoparia.  He  re- 
marks: “The  rather  flat,  slipper-shaped  glabella  is  tapering  and  slightly 
acuminated  anteriorly,  with  a faint  ridge  on  the  median  line ; two  small 
and  very  superficial  depressions  and  a posterior  faint  furrow  very  partially 
divide  the  glabella.  The  facial  sutures  run  nearly  parallel  to  the  margin  of 
the  glabella  and  join  a thickened,  cord-like  anterior  narrow  border,  inclos- 
ing a convex  area,  narrower  in  front  than  at  the  sides.  Oblique  plications 
can  sometimes  be  traced  on  the  cheek-plate  in  advance  of  the  eye,  converg- 
ing towards  the  apex  of  the  glabella.”  He  refers  the  following  figures  to  the 
genus:  Plate  1,  fig.  8,  Crepicephalus ?,  pygidium  from  the  Miniskah  Trilobite 
grit.  Plate  1,  fig.  13,  Crepicephalus?  wisconensis  (n.  s. ),  part  of  cephalothorax 
and  a portion  of  the  cephalic  shield  of  D.  granulosus  ?.  Plate  1 a,  fig.  10, 
glabella  of  Crepicephalus  n.  g.,  near  Miniskah.  Plate  la,  fig.  14,  pygidium 
of  Crepicephalus?  miniscaenis  n.  s.,  from  Miniskah  grits.  Plate  1 a,  fig.  16, 
pygidium  and  portion  of  Crepicephalus  (?)  and  portions  of  cephalothorax  of 
that  genus,  from  the  Miniskah  Trilobite  grit.  Plate  la,  fig.  18,  glabella  of 
Crepicephalus,  near  Miniskah,  Mississippi  River. 

[ Bathyurus  ?]  angulatus  Hall  and  Whitfield.  (See  Ptychoparia  angulatus.) 

[Loganellus]  anyius  Hall  and  Whitfield.  (See  Ptychoparia  anytus.) 

[Loganellus]  centralis  Whitfield.  (See  Ptychoparia  oweni.) 

gibbsi  Whitfield,  1880  ; Ann.  Rept.  Geol.  Survey  Wisconsin,  1879,  p.  50. 

Potsdam. 

gibbsi  Whitfield,  1880 ; Geol.  Wisconsin,  vol.  2,  p.  67. 

gibbsi  Whitfield,  1882;  Geol.  Wisconsin,  vol.  4,  p.  184,  pi.  10,  figs.  12, 13. 

[Loganellus]  granulosa  Hall  and  Whitfield.  (Sec  Ptychoparia  granulosa.) 

[Loganellus]  haguei.  (See  Lisostracus  haguei  and  Ptychoparia  haguei. ) 

[ Loganellus]  maculosus  Hall  and  Whitfield.  (See  Ptychoparia  maculosus.) 

[Loganellus]  montanensis  Whitfield.  (See  Ptychoparia  montanensis.) 

[Loganellus]  nitidens  Hall  and  Whitfield.  (See  Ptychoparia  nitidens.) 

onustus  Whitfield,  1878;  Ann.  Rept.  Geol.  Survey  Wisconsin,  1877,  p.  53. 

Potsdam. 

onustus  Whitfield,  1882;  Geol.  Wisconsin,  vol.  4,  p.  182,  pi.  1,  figs.  22,23. 

oweni.  (See  Agraulos  oweni  and  Ptychoparia  oweni.) 

[Loganellus]  planus  Whitfield.  (See  Ptychoparia  planus.) 

[Loganellus]  quadrans  Hall  and  Whitfield.  (See  Ptychoparia  quadrans.) 

[Loganellus]  simulator  Hall  and  Whitfield.  (See  Ptychoparia  nitidens.) 

[Loganellus]  unisulcatus  Hall  and  Whitfield.  (See  Ptychoparia  unisulcatus.) 

? wisconseneis  Owen.  (See  Anomocare  wisconsensis.) 

Crepicephalus  Walcott,  1884;  Bull.  U.  S.  Geol.  Survey,  No.  10,  p.  35. 

Type,  Dikelocephalus ? io  wen  sis  Owen. 


106 


A BIBLIOGRAPHY  OF  PALEOZOIC  CRUSTACEA. 


[bull.  63. 


Crepicephalus  augusta  Walcott,  1886;  Bull.  U.  S.  Geol.  Survey,  No.  30,  p.  208,  pi. 
28,- figs.  2,  2 a,  b.  Middle  Cambrian. 

[ Dikelocephalus?]  iowensis  Oweu,  1852;  Rept.  Geol.  Wisconsin,  Iowa,  and 

Minnesota,  p.  575,  pi.  1,  fig.  4 ; pi.  1 a,  fig.  13.  Potsdam. 

Undetermined  Trilobite  Owen,  1848 ; Rept.  Geol.  Reconnoissance  Chippewa 
Land  Dist.,  p.  14,  pi.  7,  fig.  1. 

[ Conocephalites ] iowensis  Shumard,  1863;  Trans.  Acad.  Sci.  St.  Louis,  vol.  2, 

p.  102. 

[Conocephalites]  iowensis  Hall,  1863;  16th  Rept.  New  York  State  Cab.  Nat. 

Hist.,  p.  162,  pi.  7,  fig.  33;  pi.  8,  figs.  10-12  and  30. 

iowensis  Walcott,  1884;  Bull.  U.  S.  Geol.  Survey,  No.  10,  p.  36. 

iowensis  Walcott,  1886  ; Bull.  U.  S.  Geol.  Survey,  No.  30,  p.  207. 

liliana  Walcott,  1886 ; Bull.  U.  S.  Geol.  Survey,  No.  30,  p.  209,  pi.  28,  figs.  3, 

3 a,  c.  Middle  Cambrian. 

Cryphceus  Green,  1837;  Am.  Jour.  Sci.,  1st  series,  vol.  32,  p.  343. 

Type,  Cryphceus  boothi  Green. 

[ Dalmanites  ( Cryphceus )]  barrisi  Hall,  1888;  Pal.  New  York,  vol.  7,  p.  48,  pi.  16  a, 

fig.  18.  Hamilton. 

boothi  Green,  1837;  Am.  Jour.  Sci.,  1st  series,  vol.  32,  p.  343,  figure.  Hamilton. 

Syn.,  Cryphceus  cjrceni  Courad,  1839;  2d  Ann.  Rept.  Pal.  Dept.  New  York  Geol. 
Survey,  p.  66. 

Cryphceus  calliieles  Conrad,  1839  ; 2d  Ann.  Rept.  Pal.  Dept.  New  York  Geol. 
Survey,  p.  62. 

Asaphus  lialli  Conrad,  1840;  3d  Ann.  Rept.  Pal.  Dept.  New  York  Geol.  Sur- 
vey, p.  204. 

Cryphceus  calliteles  Hall,  1843;  Geol.  New  York,  pt.  4,  p.  201. 

Cryphceus  calliteles  De  Verneuil,  1850;  Bull.  Soc.  G6ol.  France,  2d  series, 
vol.  7,  p.  164,  pi.  1,  fig.  3. 

Pliacops  peclinatus  F.  A.  Roemer,  1850;  Beitriige  zur  Kenntn.  Harzgeb.,  p. 
62,  pi.  9,  fig.  27. 

Dalmania  calliteles  Emmons,  1860;  Manual  Geology,  p.  138,  fig.  124  (7). 

[ Dalmania ] boothi  Hall,  1861 ; Des.  New  Species  of  Fossils,  p.  63. 

[Dalmania]  boothi  Hall,  1862 ; 15th  Rept.  NeAv  York  State  Cab.  Nat.  Hist.,  p.  91. 

[ Dalmanites ] boothi  Hall,  1876;  Ulus.  Devonian  Foss.,  pi.  16,  figs.  1-6,  9-11, 

13,  15,  16. 

Syn.,  Cryphceus  stellifer  Kayser,  1878;  Abhandl.  geol.  Specialkarte  Pr.,  vol.  2, 
pt.  4,  p.  33,  (in  part). 

Cryphceus  laciniatus  Kayser,  1878;  idem.,  p.  34. 

[ Dalmanites  (Cryphceus)]  boothi  Hall,  1888;  Pal.  New  York,  vol.  7,  p.  42,  pi.  16, 

figs.  1-4  ; pi.  16  a,  figs.  3-8. 

callitelus  Green,  1837 ; Am.  Jour.  Sci.,  1st  series,  vol.  32,  p.  346. 

Hamilton. 

[ Dalmanites ] boothi  Hall,  1876;  Illus.  Devonian  Foss.,  pi.  16,  figs.  7,  8,  12,  14. 

(?)  callitelus  Kayser,  1878  ; Abhandl.  geol.  Specialkarte  Pr.,  vol.  2,  pt.  4,  p.  32, 

pi.  3,  tig.  10. 

[ Dalmanites  ( Cryphceus )]  boothi  var.  calliteles  Hall  and  Clarke,  1888;  Pal. 

New  York,  vol.  7,  p.  45,  pi.  16,  figs.  5-22 ; pi.  16  a,  figs.  9-17. 

[Dalmanites  (Cryphceus)]  comis  Hall,  1888;  Pal.  New  York,  vol.  7,  p.  41,  pi. 

16  a,  fig.  1.  Corniferous. 

[Dalmania]  pleione  Hall,  1861  ; Des.  New  Species  Fossils,  p.  62.  Hamilton. 

[Dalmania]  pleione  Hall,  1862;  15th  Rept.  New  York  State  Cab.  Nat.  Hist., 

p.  90. 

[Dalmanites]  pleione  Hall,  1876;  111ns.  Devonian  Foss.,  pi.  16,  fig.  17. 

pleione  Kayser,  1878;  Abhandl.  geol.  Specialkarte  Pr.,  vol.  2,  pt.  4,  p.  33. 


VOGDE8.] 


CATALOGUE  OF  TRILOBITES. 


107 


Cryphaeus  [ Dalmanites,  (Cfyphrens)^  pleione  Hall,  18.88;  Pal.  New  York,  voL  7,  p. 
41,  pi.  16  a,  tig.  2. 

Cryptolithus  Green,  1832;  Mon.  Tril.  North  America,  p.  72. 

This  generic  should  replace  that  of  Trinucleus  Murch.,  1839. 

Cryptonymus  Eichwald,  1825  ; Syn.  to  Jsaphus,  Illcenus,  and  Niobe. 

Cryptonymus  Eichwald,  1840.  (See  Encrimirus.) 

Cybele  Loven,  1845;  Svenska  Yetensk.  Akad.  Forliandl.,  p.  110. 

Type,  Cybele  bellatula  Dalman. 

punctata  Hall.  (See  Encrinurus  ornatus.) 

Cyphaspis  Burmeister,  1843;  Org.  Trilobiten,  p.  98. 

Type,  Cyphaspis  ceratopthahna  Burmeister. 

christyi  Hall,  1863;  Trans.  Albany  Inst.,vol.  4,  p.  220.  Niagara. 

christyi  Hall,  1875;  28th  Rept.  New  York  State  Mus.  Nat.  Hist.,  pi.  32,  figs.  5-7. 

christyi  Hall,  1879  ; 28th  Rept.  New  York  State  Mus.  Nat.  Hist.,  p.  188,  pi.  32, 

figs.  5-7. 

- — christyi  White,  1880;  2d  Ann.  Rept.  Dept. -Statistics  and  Geol.  Indiana,  p. 
493,  pi.  3,  fig.  9. 

christyi  Hall,  1882 ; 11th  Ann.  Rept.  Dept.  Geol.  Nat.  Hist.  Indiana,  1881,  p.  333, 

pi.  34,  figs.  5-7. 

coelebs  Hall,  1888 ; Pal.  New  York,  vol.  7,  p.  151,  pi.  24,  fig.  1. 

Lower  Helderberg. 

craspedota  Hall,  1888 ; Pal.  New  York,  vol.  7,  p.  148,  pi.  24,  figs.  15-20. 

Hamilton. 

diadema  Hall,  1888;  Pal.  New  York,  vol.  7,p.  144,  pi.  24,  fig.  13. 

Upper  Helderberg. 

girardeauensis  Shumard,  1855  ; 1st  and  2d  Rept.  Geol.  Missouri,  p.  197,  pi.  B, 

fig.  11  a,  b. 

girardeauensis  Emmons,  1860  ; Manual  Geology,  p.  159,  fig.  145  (2). 

hybrida  Hall,  1888;  Pal.  New  York,  vol.  7,  p.  144,  pi.  24,  fig.  14. 

Upper  Helderberg. 

[ Phillipsia ] laevis  Hall,  1876;  Illus.  Devonian  Foss.,  pi.  21,  fig.  29. 

laevis  Hall,  1888;  Pal.  New  York,  vol.  7,  p.  150,  pi.  21,  fig.  29.  Chemung. 

[ Phillipsia ] minuscula  Hall,  1876;  Illus.  Devonian  Foss.,  pi.  20,  fig.  17. 

Upper  Helderberg. 

minuscula  Hall,  1888 ; Pal.  New  York,  vol.  7,  p.  140,  pi.  20,  fig.  17 ; pi.  24,  figs.  7-12. 

[Phillipsia?  ( Brachymetopus?)~\  ornata  Hall,  1876;  Illus.  Devonian  Foss.,  pi.  21, 

fig.  1.  Hamilton. 

Syn.,  Phillipsia  coronata  Miller,  1877;  Catalogue  Am.  Pal.  Foss.,  p.  221. 

Phillipsia  coronata?  Walcott,  1884 ; Pal.  Eureka  Dist.,  Mon.  U.  S.  Geol.  Sur- 
vey, vol.  8,  p.  211. 

ornata  Hall,  1888 ; Pal.  New  York,  vol.  7,  p.  145,  pi.  21,  fig.  1 ; pi.  24,  fig.  21. 

ornata  var.  baccata  Hall,  1888;  Pal.  New  York,  vol.  7,  p.  146,  pi.  24,  figs.  22,23. 

stephanophora  Hall,  1888 ; Pal.  New  York,  vol.  7,  p.  142,  pi.  24,  tigs.  2-6. 

Upper  Helderberg. 

Dalmania  Emmrich,  1844  ; Zur  Naturgoschichto  Trilobiten,  p.  15. 

This  name  having  been  used  in  1830  for  a genus  of  the  Diptera,  J.  Barrande 
suggested  that  of  Dahnanites. 

Dalmanites  (Emmrich)  Barrande,  1872;  Syst.  Sil.  Boheuio,  Suppl.,  vol.  1,  p.  27. 
Type,  JJalmanites  caudatus  Biinnich. 

Syn.,  Pleuracanlhus  Milne-Ed wards,  1840;  Crnst.,  vol.  3,  p.  329. 

Odontochilc  Corda,  1847 ; Prodr.,  p.  208,  pi.  5,  lig.  56. 

Ostcropyye  Corda,  1847  ; Prodr.,  p.  241,  pi.  6,  fig.  66. 

Metacanthus  Corda,  1817;  Prodr.,  p.212,  pi.  6,  fig.  67. 

Chasmops  McCoy,  1849;  Annals  Nat.  Hist.,  2d  series,  vol.  4. 


108 


A BIBLIOGRAPHY  OF  PALEOZOIC  CRUSTACEA. 


[bull.  63 


s.yn.,  Cryphwus  Green,  1837;  Am.  Jour.  Sci.,  1st  series,  vol.  32, p.  343. 

Odontocephalus  Conrad,  1840;  3d  Kept.  Pal.  Dept,  New  York  Geol.  Survey 
p.  204.  J 

Hausmavnia  Hall,  1888 ; Pal.  New  York,  vol.  7,  p.  xxxi. 

Coronura  Hall,  1888 ; Pal.  New. York,  vol.  7,  p.  xxxii. 

Corycephalus  Hall,  1888 ; Pal.  New  York,  vol.  7,  p.  xxxiv. 

Dalmanites  [Asaphus  ?]  acantholeurus  (Conrad)  Hall,  1862;  15th  Rept.  New  Yort 
State  Cab.  Nat.  Hist.,  p.  113. 

[Asaphus  S']  acantholeurus  Conrad,  1841 ; 4th  Rept.  Pal.  Dept.  New  York  Geol 
Survey  p.  48.  Onondaaa 

acantholeurus  Hall,  1876;  Ulus.  Devonian  Foss.  Crust.,  pi.  19, fig  14 

[Dalmamtes]  acantholeurus  Hall,  1876;  Ulus.  Devonian  Foss.  Crust.,  pi  19 

fig.  14.  ’ ! 

achates  Billings,  1860 ; Canadian  Naturalist,  vol.  5,  p.  63,  fig.  9.  Trenton 

achates  Billings,  1863;  Geol.  Canada,  p.  187,  fig.  186. 

aegeria  Hall,  1861 ; Des.  New  Species  Fossils,  p.  57.  Upper  Helderbero- 

aegeria  Hall,  1862 ; 15th  Rept.  New  York  State  Cab.  Nat.  Hist.,  p.  85. 

■ aegeria  Hall,  1876;  Ulus.  Devonian  Foss.  Crust.,  pi.  12,  figs.  1,2,7. 
aegeria  Hall,  1876;  Illus.  Devonian  Foss.  Crust.,  p.  12,  figs  3,  6,  8 (not  figs 
1, 2,  7). 

[Odontocephalus]  aegeria  Meek  and  Worthen,  1868;  Geol.  Illinois  vol  3 p 417 

pi.  10,  figs.  4 a,  b,  c.  * 

[ Odontocophalus ] aegeria  Hall,  1888 ; Pal.  New  York,  vol.  7,  p.  53,  pi.  11  b,  figs 

[ Calymene ] anchiops  Green,  1832;  Monthly  Am.  Jour.  Geol.,  vol.  1,  p.  558. 

r_  7 Upper  Helderberg. 

[ Calymene ] anchiops  Green,  1832;  Mon.  Tril.  N.  A.,  p.  35,  cast  7. 

Syn.,  Asaphus  lalicostatus  Green,  1832;  Monthly  Am.  Jour.  Geol.,  vol.  1,  p.  559, 
Asaphus  laticostatus  Green,  1832;  Mon.  Tril.  N.  A.,  p.  45,  cast  13.  * 

[Phacops]  anchiops  Burmeister,  1843  ; Org.  Trilobiten,  p.  90  (Ray  Soc.  edition) 

[Phacops]  anchiops  Hall,  1851;  Rept.  Geol.  Lake  Superior  Land  Dist.  (Foster 

and  Whitney),  pt.  2,  p.  224,  pi.  35,  figs.  3 a,  3 b.  (See  Dalmanites  anchiops 
var.  armatus.) 

[DalmanW]  anchiops  Hal],  1861 ; Des.  New  Species  Fossils,  p.  55. 

IDalmanm-]  anchiops  Hall,  1862;  15th  Rept.  New  York  State  Cab.  Nat.  Hist. 

p.  83. 

anchiops  Hall,  1876;  Ulus.  Devonian  Foss.  Crust.,  p.  9,  fio-g.  1 3_6  9 10  12 
13 ; pi.  10,  figs.  6-14. 

[Chasmops]  anchiops  Hall,  1888;  Pal.  New  York,  vol.  7,  p.- 59  pi  9 fio-s  1-6 

10,  12,  13;  pi.  10,  figs.  1-14.  * * ' - 

[Dalmania]  anchiops  var.  armatus  Hall,  1861 ; Des.  New  Species  Foss.,  p.  56. 

[Dalmania]  anchiops  var.  armatus  Hall,  1862;  15th  Rept.  New  York  State 

Cab.  Nat.  Hist.,  p.  84. 

anchiops  var.  armatus  Hall,  1876;  Illus.  Devonian  Foss.  Crust.,  pi.  9,  figs.  2, 

7,  8. 

[Chasmops]  anchiops  var.  armatus  Hall,  1888;  Pal.  New  York,  vol  7 p 62  nl 

9,  figs.  7-9;  pi.  10,  fig.  14.  ' ’ P* 

[Chasmops]  anchiops  var.  sobrinus  Hall,  1888;  Pal.  New  York,  vol.  17,  p 62 

pi.  9,  fig.  11.  f f ) 

[Odontocephalus]  arenarius  Meek  and  Worthen,  1868 ; Geol.  Survey  Illinois,  vol. 

3,  p.  417,  pi.  9,  fig.  10.  (See  Dalmanites  selenurus.) 

[Asaphus]  aspectans  Conrad,  1841;  5th  Ann.  Rept,  Pal.  Dept.  New  York  Geol 

Survey,  p.  48,  fig.  9.  Upper  Helderberg. 

Syn.,  Asaphus?  denticulatus  Conrad;  idem.,  p.  48. 


CATALOGUE  OF  TRILOBITES. 


VOGDES.] 


109 


Dalmanites  [Dalmania\  aspectans  Hall,  1861;  Des.  New  Species  Foss.,  p.  60  (in 
error  D.  adspectans). 

[ Dalmania ] aspectans  Hall,  1862 ; 15tli  Rept.  New  York  State  Cab.  Nat.  Hist., 

p.  88  (in  error  D.  adspectans). 

Syn.,  Dalmania  helena  Hall,  1861 ; Des.  New  Species  Foss.,  p.  61. 

Dalmania  helena  Hall,  1862 ; 15th  Rept.  New  York  State  Cab.  Nat.  Hist., 
p.  89. 

Dalmanites  ohioensis  Meek,  1871 ; Proc.  Acad.  Nat.  Sci.  Phila.,  p.  91. 
Dalmanites  ohioensis  Meek,  1873 ; Pal.  Ohio,  vol.  1,  p.  234,  pi.  23,  fig.  1. 
Dalmanites  denticulatus  Hall,  1876;  Illus.  Devonian  Foss.  Crust.,  pi.  10, 

fig.  1. 

aspectans  Hall,  1876 ; Illus.  Devonian  Foss.  Crust.,  pi.  13,  figs.  6-8. 

Syn.,  helena  Hall,  1876 ; Illus.  Devonian  Foss.  Crust.,  pi.  13,  figs.  13,  14. 

[ Coronura ] aspectans  Hall,  1888;  Pal.  New  York,  vol.  7,  p.  33,  pi.  12,  figs. 

1-11,  13. 

[ Cryphceus ] barrisi  Hall.  (See  Cryphaeus  barrisi  Hall.) 

bebryx  Billings,  1860;  Canadian  Naturalist,  vol.  5,  p.  62,  fig.  8.  Trenton. 

bebryx  Billings,  1863;  Geol.  Canada,  p.  187,  fig.  185. 

[Dalmania]  bifida  Hall,  1861 ; Des.  New  Species  Foss.,  p.  63.  Upper  Helderberg. 

[ Dalmania ] bifida  Hall,  1862;  15th  Rept.  New  York  State  Cab.  Nat.  Hist.,  p. 

91. 


[ Odontocephalus ] bifida  Hall  and  Clarke,  1888;  Pal.  New  York,  vol.  7,  p.  53,  pi, 

11  b,  figs.  22-25. 

Compare  Dalmanites  cegeria  Hall. 

[ Dalmania ] boothi.  (See  Cryphaeus  boothi  Green.) 

bicornis  Hall,  1875;  28th  Rept.  New  York  State  Mus.  Nat.  Hist.  Expl.,  pi.  33, 

fig*  18.  Niagara. 

bicornis  Hall,  1879;  28th  Rept.  New  York  State  Mus.  Nat.  Hist.,  p.  196,  pi.  33, 

fig.  18. 

bicornis  Hall,  1882;  11th  Aun.  Rept.  Geol.  Nat.  Hist.  Indiana,  1881,  p.  342,  pi. 

35,  fig.  18. 

breviceps  Hall,  1866;  24th  Rept.  New  York  State  Mus.  Nat.  Hist.,  p.  223,  pi.  8, 

figs.  15, 16.  Hudson. 

breviceps  Miller,  1874;  Cincinnati  Quart.  Jour.  Sci.,  vol.  1,  p.  143. 

breviceps  Hall  and  Whitfield,  1875 ; Pal.  Ohio,  vol.  2,  p.  108,  pi.  4,  figs.  15, 

16. 


[ Phacops ] callicephalus  Hall,  1847;  Pal.  New  York,  vol.  1,  p.  247,  pi.  65,  figs. 

3a-3i.  Trenton. 

[Phacops]  callicephalus  Hall,  1851;  Rept.  Geol.  Lake  Superior  Land  Dist. 

(Foster  and  Whitney),  vol.  2,  p.  212,  pi.  3,  figs.  3 a,  3 b. 

[ Phacops']  callicephalus  Emmons,  1855;  Am.  Geology,  vol.  1,  pt.  2,  p.  214,  pi. 

15,  figs.  7, 7 a. 

[ Dalmania]  calliteles.  (See  Cryphaeus  calliteles). 

[ Dalmania ] calypso  Hall,  1861 ; Des.  New  Species  Foss.,  p.  61. 

Upper  Helderberg. 

[Dalmania]  calypso  Hall,  1862;  15th  Rept.  New  York  State  Cab.  Nat.  Hist., 

p.  89. 


calypso  Hall,  1876;  Illus.  Devonian  Foss.  Crust.,  pi.  13,  figs.  1,2. 

[Cliasmops]  calypso  Hall,  1888;  Pal.  New  York,  vol.  7,  p.  4,  pi.  16a,  fig.  1. 

? cayahogoe  Claypole,  1884;  Geol.  Mag.,  vol.  1,  p.  305,  figure.  Carboniferous. 
? cayahogoe  Woodward,  1884;  Mon.  Brit.  Carboniferous  Tril.,  p.  79,  figure. 

carleyi  Meek,  1872;  Am.  Jour.  Sci.,  3d  series,  vol.  3,  p.  424.  Hudson. 

— — carleyi  Meek,  1873;  Pal.  Ohio,  vol.  1,  p.  170,  pi.  14,  iigs.  2a-2d. 

carleyi  Miller,  1871 ; Cincinnati  Quart.  Jour.  Sci.,  vol.  1,  p.  142. 

— — [ Dalmania ] eaudata  (Brong.)  Roomer.  (Soo  Dalmanites  limulurus  Green.) 


110 


A BIBLIOGRAPHY  OF  PALEOZOIC  CRUSTACEA. 


[bull.  63. 


Dalmanites  [ Crijpliceus ] comis.  (See  Cryphseus  comis  Hall.) 

concinnus  Hall,  1876  ; Illus.  Devonian  Foss.  Crust.,  pi.  10,  figs.  3-5.  Schoharie. 

[ Raxismannia ] concinnus  Hall,  1888 ; Pal.  New  York,  vol.  7,  p.  30,  pi.  11  a,  figs. 

9-11. 

[ Hausmannia ] concinnus  var.  serrula  Hall  and  Clarke,  1888;  Pal.  New  York, 

vol.  7,  p.  30,  pi.  11  a,  fig.  12. 

[ Dalmania ] coronatus  Hall,  1861 ; Des.  New  Species  Foss.,  p.  58. 

Upper  Helderberg. 

[Dalmania']  coronatus  Hall,  1862;  15th  Rept.  New  York  State  Cab.  Nat.  Hist., 

p.  86. 

coronatus  Hall,  1876 ; Illus.  Devonian  Foss.  Crust.,  pi.  12,  figs.  15-17 ; pi.  13, 

fig.  5. 

[Odontocephalus  ?]  coronatus  Hall,  1888;  Pal.  New  York,  vol.  7,  p.  54,  pi.  11  b, 

figs.  12-14. 

danae  Meek  and  Worthen,  1865;  Pros.  Acad.  Nat.  Sci.  Phila.,  p.  264.  Niagara. 

danae  Meek  and  Worthen,  1868 ; Pal.  Illinois,  vol.  3,  p.  363,  pi.  6,  figs.  1 a-1  f. 

dentata  Barrett,  1876 ; Am.  Jour.  Sci.,  3d  series,  vol.  11,  p.  200,  plate. 

Lower  Helderberg. 

dentata  Barrett,  1876;  Am.  Jour.  Sci.,  3d  series,  vol.  12,  p.  70. 

[ Corycephalus]  dentatus  Hall  and  Clarke,  1888;  Pal.  New  York,  vol.  7,  p.  58, 

pi.  11  a,  figs.  4-6. 

[ Asaphus? ] denticulatus  Conrad,  1841;  5th  Rept.  Pal.  Dept.  New  York  Geol. 

Survey,  p.  48. 

Lower  Helderberg. 

denticulatus  Hall,  1876;  Illus.  Devonian  Foss.  Crust.,  pi.  10,  fig.  1. 

[ Phceton ] denticulatus  Meek,  1877 ; U.  S.  Geol.  Expl.  40th  Par.,  vol.  4,  p.  49, 

pi.  1,  figs.  10  a,  b. 

emarginatus  Hall,  1876;  Illus.  Devonian  Foss.  Crust.,  pi.  10,  fig.  2.  . 

Upper  Helderberg. 

[Coronura]  emarginatus  Hall,  1888;  Pal.  New  York,  vol.  7,  p.  40,  pi.  11  a,  figs. 

7,  8. 

epicrates  Billings,  1863 ; Proc.  Portland  Soc.  Nat.  Hist.,  vol.  1,  p.  119,  pi.  1,  fig.  21. 

[Dalmania]  erina  Hall,  1861 ; Des.  New  Species  Foss.,  p.  62. 

Upper  Helderberg. 

[Dalmania]  erina  Hall,  1862;  15th  Rept.  New  York  State  Cab.  Nat.  Hist.,  p.  90. 

erina  Hall,  1876 ; Illus.  Devonian  Foss.  Crust.,  pi.  13,  figs.  3,  4. 

[Chasmops]  erina  Hall,  1888;  Pal.  New  York,  vol.  7,  p.  67,  pi.  11,  figs.  16-18. 

Upper  Silurian. 

[Dalmania]  helena.  (See  Dalmanites  aspectans.) 

intermedius  Walcott,  1877;  Advance  sheets  31st  Rept.  New  York  State  Cab. 

Nat.  Hist.,  p.  17.  Trenton. 

intermedius  Walcott,  1879;  31st  Rept.  New  York  State  Cab.  Nat.  Hist.,  p.  69. 

[Phacopsf]  laticauda  Hall,  1847 ; Pal.  New  York,  vol.  1,  p.  248,  pi.  64,  fig.  3. 

[Asaphus]  limulurus  Green,  1832;  Monthly  Am.  Jour.  Geol.,  vol.  1,  p.  559. 

Niagara. 

[Asaphus]  limulurus  Green,  1832;  Mon.  Tril.  N.  A.,  p.  48,  cast  16. 

[Phacops]  limulurus  Hall,  1852;  Pal.  New  York,  vol.  2,  p.  303,  pi.  67,  figs.  1-8. 

Syn.  [Dalmania]  caudata  (Brong.)  Roemer,  1860;  Die  sil.  Fauna  W.  Tenn..p.  82, 
pi.  5,  fig.  21. 

[Dalmania]  logani  Hall,  1860;  Canadian  Naturalist,  vol.  5,  p.  156,  fig.  18.  ' 

Silurian. 

[Dalmania]  macrops  Hall,  1861 ; Des.  New  Species  Foss.,  p.  59. 

Upper  Helderberg. 

[Dalmania]  macrops  Hall,  1862;  15th  Rept.  New  York  State  Cab.  Nat.  Hist., 

p.  87. 


VOGDKS.] 


CATALOGUE  OF  TR1LOB1TES. 


Ill 


Dalmanites  macrops,  1876 ; Illus.  Devonian  Foss.  Crust.,  pi.  13,  figs.  9, 10. 

[ Chasmops ] macrops  Hall,  1888;  Pal.  New  York,  vol.  7,  p.  68,  pi.  11  a,  figs. 

14, 15. 

macroura  ? (Sjogr.)  Billings,  1866;  Catalogue  Sil.  Foss.  Anticosti,  p.  61. 

[ Dal  mania ] meta  Hall,  1862;  Geol.  Wisconsin,  vol.  1,  p.  433. 

meeki  Walcott,  1884;  Pal.  Eureka  Dist.,  Mon.  U.  S.  Geol.  Survey,  vol.  8,  p.  207, 

pi.  17,  figs.  5-5  a,  b (not  fig.  5 c). 

(undetermined  sp.)  Meek,  1877 ; U.  S.  Geol.  Expl.  40th  Par.,  vol.  4,  p.  48,  pi.  1, 

figs.  11,  11  a. 

[ Hausmannia ] meeki  Hall,  1888 ; Pal.  New  York,  vol.  7,  p.  11  a,  figs.  28-30. 

lAsaphus]  micrurus  Green,  1832;  Monthly  Am.  Jour.  Geology,  p.  559,  pi.  14, 

fig.  3.  Lower  Helderberg. 

[ Asaphus ] micrurus  Green,  1832  ; Mon.  Tril.  N.  A.,  p.  56,  cast  19,  pi.,  fig.  3. 

.{Dalmania ] micrurus  Hall,  1859  ; Pal.  New  York,  vol.  3,  p.  359,  pi.  75,  figs.  13-18. 

\_AsapTius']  myrmecophorus  Green,  1835;  Am.  Jour.  Sci.,  1st  series,  vol.  23,  p. 

397.  Upper  Helderberg. 

[Asaphus ] myrmecophorus  Green,  1835;  Suppl.  Mon.  Tril.  N.  A.,p.  16,  cast  40. 

[J Dalmania]  myrmecophorus  Hall,  1861;  Des.  New  Species  Foss.,  p.  60. 

[ Dalmania ] myrmecophorus  Hall,  1862  ; 15th  Kept.  New  York  State  Cab.  Nat. 

Hist.,  p.  88. 

myrmecophorus  Hall,  1876;  Illus.  Devonian  Foss.  Crust.,  pi.  13,  figs.  15, 16. 

[Coronura]  myrmecophorus  Hall,  1888 ; Pal.  New  York,  vol.  7,  p.  37,  pi.  11  a, 

fig.  13  ; pi.  13,  fig.  12;  pi.  14,  figs.  1-6 ; pi.  15,  figs.  1-4. 

[Asaphus]  nasutus  Conrad,  1841 ; 5th  Kept.  Pal.  Dept.  New  York  Geol.  Survey, 

p.  48.  Lower  Helderberg. 

[ Dalmania ] nasutus  Hall,  1859 ; Pal.  New  York,  vol.  3,  p.  362,  pi.  75,  fig.  2 ; 

pi.  76,  figs.  1-9. 

[ Dalmanites']  ohioensis.  (See  Dalmanites  aspectans.) 

[ Hausmannia ] phacoptyx  Hall,  1888;  Pal.  New  York,  vol.  7,  p.  31,  pi.  11  a, 

figs.  23-29.  Upper  Helderberg. 

[Dalmania]  pleione.  (See  Cryphaeus  pleione.) 

[Asaphus]  pleuropteryx  Green,  1832;  Monthly  Jour.  Geol.,  vol.  1,  p.  559. 

Lower  Helderberg. 

[ Asaplius ] pleuropteryx  Green,  1832;  Mon.  Tril.  N.  A.,  p.  55,  cast  18. 

[ Dalviania ] pleuropteryx  Hall,  1859;  Pal.  New  York,  vol.  3,  p.  356,  pi.  74,  figs. 

5 (?)  9 (?)  (not  figs.  1-4,  6-8,  10-12),  pi.  75,  fig.  1. 

[Hausmannia]  pleuropteryx  Hall,  1888;  Pal.  New  York,  vol.  7,  p.  28,  pi.  9, 

> figs.  1-3. 

— — [ Corycephalus ] pygmaeus  Hall,  1888;  Pal.  Now  York,  vol.  7,  p.  56,  pi.  11,  figs. 
5-8.  Upper  Helderberg. 

regalis  Hall,  1876;  Illus.  Devonian  Foss.  Crust.,  pi.  11,  figs.  1-4. 

Upper  Helderberg. 

- — [Corycephalus]  regalis  Hall,  1888;  Pal  New  York,  vol.  7,  p.  55,  pi.  11, figs.  1-4. 

[ Asaplius ] selenurus  Eaton,  1832;  Geological  Text  Book,  pi  31,  pi.  1,  fig.  1. 

Upper  Helderberg. 

[Asaphus]  selenurus  Green,  1832 ; Mon.  Tril.  N.  A.,  p.  46,  casts  14  and  15. 

Syn.,  Calymene?  odontocephala  Green,  1835;  Suppl.  Mon.  Tril.  N.  A.,  p.  9,  cast  36. 
Calymenef  odontocephala  Green,  1835;  Am.  Jour.  Sci.,  1st  series,  vol.  25,  p. 
334. 

[Odontocephalus]  selenurus  Conrad,  1840;  3d  Rept.  Pal.  Dept.  New  York  Geol. 

Survey,  p.  204. 

[Odontocephalus]  selenurus  Vanuxom,  1842;  Geol.  New  York,  3d  Geol.  Dist., 

pp.  139, 140,  fig.  1. 

[Odontocephalus]  selenurus  Hall,  1843;  Geol.  Now  York,  4th  Geol.  Dist.,  p.  175, 

fig.  1. 


112 


A BIBLIOGRAPHY  OF  PALEOZOIC  CRUSTACEA. 


[bull.  63. 


Dalmanites  [ Dalmania ] selenurus  Hall,  1859 ; 12th  Rept.  New  York  State  Cab. 
Nat.  Hist.,  p.  88. 

[ Dalmania ] selenurus  Hall,  1861;  Des.  New  Species  Foss.,p.  56. 

[ Dalmania ] selenurus  Hall,  1862 ; 15th  Rept.  New  York  State  Cab.  Nat.  Hist., 

p.  84. 

Syn.,  Odontocephalus?  ( Dalmanites-Odontocephalus ) arenarius  Meek  and  Worthen, 
1868;  Geol.  Survey  Illinois,  vol.  3,  p.  416,  pi.  9,  fig.  10. 

selenurus  Hall,  1876;  Illus.  Devonian  Foss.  Crust.,  pi.  12,  figs.  12-14. 

[Odontocephalus ] selenurus  Hall,  1888;  Pal.  New  York,  vol.  7,  p.  49,  pi.  11  b,  figs. 

15-21 ; pi.  12,  figs.  1-13. 

[Dalmania]  tridens  Hall,  1859;  Pal.  New  York,  vol.  3,  p.  361,  pi.  75,  figs.  3-6. 

Lower  Helderberg. 

[ Dalmania ] tridentifera  Shumard,  1855;  1st  and  2d  Geol.  Repts.  Missouri, 

p.  199,  pi.  B,  figs.  8 a-c.  Lower  Helderberg. 

tridentifera  Meek  and  Worthen,  1868;  Pal.  Illinois,  vol.  3,  p.  391,  pi.  7,  fig.  16. 

troosti  Safford,  1869;  Geol.  Tennessee,  p.  290.  (See  Chasmops  troosti  Safford.) 

Nashville. 

[Dalmania]  verrucosus  Hall,  1863;  Trans.  Albany  Inst.,  vol.  4,  p.  218.  (Ab- 
stract published  May,  1863,  p.  24.)  Niagara. 

verrucosus  Hall,  1875;  28th  Rept.  New  York  State  Mus.  Nat.  Hist.,  pi.  23,  figs. 

5-17,  13-15.  Museum  ed.,  1879,  p.  195,  pi.  23,  fig.  5-17;  pi.  34,  figs.  13-15. 

verrucosus  Hall,  1882;  11th  Ann.  Rept.  Dept.  Geol.  Nat.  Hist.  Indiana,  p.  341, 

pi.  35,  figs.  5-17;  pi.  36,  figs.  13-15. 

vigilans  Hall,  1861 ; Rept.  Progress  Wisconsin  Geol.  Survey,  p.  51.  Niagara. 

[ Dalmania 3.  vigilans  Hall,  1867 ; 20th  Rept.  New  York  State  Cab.  Nat.  Hist., 

p.  335,  pi.  21,  figs.  16-18. 

[Dalmania]  vigilans  Hall,  1870;  20th  Rept. New  York  State  Cab.  Nat.  Hist.  (2d 

ed.),  p.  426,  pi.  21,  figs.  16-18. 

vigilans  Hall,  1875;  28th  Rept.  New  York  State  Mus.  Nat.  Hist.  Expl.,  pi.  33, 

figs.  1-4. 

vigilans  Hall,  1879;  28th  Rept.  New  York  State  Mus.  Nat.  Hist.  (Mus.  ed.),  p. 

193,  pi.  33,  figs.  1-4. 

vigilans  Hall,  1882 ; 11th  Ann.  Rept.  Geol.  Nat.  Hist.  Indiana,  1881,  p.  339,  pi.  35, 

figs.  1-4  ; pi.  33,  fig.  9. 

werthneri  Foerste,  1885 ; Bull.  Denison  Univ.,  vol.  1,  p.  116.  Clinton. 

werthneri  Foerste,  1887  ; Bull.  Denison  Univ.,  vol.  2,  p.  109,  pi.  8,  figs.  22-25. 

Dicellocephalus.  (See  Dikelocephalus.) 

Dikelocephalus  Owen,  1852 ; Rept.  Geol.  Survey  Wisconsin,  Iowa,  and  Minnesota, 
p.  573. 

Type,  Dikelocephalus  minnesotensis  Owen. 

Syn.,  Centropleura  Angelin,  1854  ; Pal.  Scand.,  p.  87,  pi.  41,  figs.  9-11. 

This  generic  term  has  sometimes  been  spelled  Dicellocephalus. 

affinis  Billings,  1865 ; Pal.  Foss.,  vol.  1,  p.  197,  fig.  183  a,,  b.  Quebec, 

? angustifrons  Walcott,  1884  ; Pal.  Eureka  Dist.,  Mon.  U.  S.  Geol.  Survey,  vol.  8. 

p.  42,  pi.  10,  figs.  1,1  a,  b.  Cambrian. 

belli  Billings,  1860 ; Canadian  Naturalist,  vol.  5,  p.  311,  fig.  7.  Quebec. 

belli  Billings,  1865 ; Pal.  Foss.,  vol.  1,  p.  403, fig.  378. 

barabuensis  Whitfield,  1878;  Ann.  Rept.  Geol.  Survey  Wisconsin,  1877,  p.  63. 

Uower  Magnesian. 

barabuensis  Whitfield,  1882;  Geol.  Wisconsin,  vol.  4,  p.  201,  pi.  4,  figs.  6-9.  ■ 

Compare  Bathyurus  capax  Billiugs. 

bilobatus  Hall  and  Whitfield,  1877 ; U.  S.  Geol.  Expl.  40th  Par.,  p.  226,  pi.  2, 

fig.  36.  Potsdam. 

bilobatus  Walcott,  1884;  Pal.  Eureka  Dist.,  Mon.  U.  S.  Geol.  Survey,  vol.  8, 

p.  40. 


V0GDE3.] 


CATALOGUE  OF  TRILOB1TES. 


113 


Dikelocephalus  crassimarginatus  Whitfield,  1882 ; Geol.  Wisconsin,  vol.  4,  p.  344, 
pi.  27,  fig.  14.  ' Potsdam. 

Syn pepinensis  (Hall),  16th  Kept.  New  York  State  Cab.  Nat.  Hist.  Expl.,  pi.  11. 
fig.  2.  • 

? corax  Billings,  1865;  Pal.  Foss.,  vol.  1,  p.  344,  figs.  322  a,  b.  Quebec. 

Referred  to  Olenoides  f corax  Walcott,  1884;  Bull.  U.  S.  Geol.  Survey,  No.  30, 
p.  184. 

cristatus  Billings,  1860 ; Canadian  Naturalist,  vol.  5,  p.  312,  fig.  10.  Quebec. 

cristatus  Billings,  1865 ; Pal.  Foss.,  vol.  1,  p.  404,  fig.  384. 

This  species  might  be  referred  to  the  genus  Dorypyge. 

devinei  Billings,  1865;  Pal.  Foss.,  vol.  1,  p.  195,  figs.  180,181.  Quebec. 

eatoni  Whitfield,  1878 ; Ann.  Rept.  Geol.  Survey  Wisconsin,  1877,  p.  65. 

Lower  Magnesian. 

eatoni  Whitfield,  1882;  Geol.  Wisconsin,  vol.  4,  p.  202,  pi.  4,  figs.  11-17;  pi.  10, 

figs.  4, 5. 

? expansus  Walcott,  1884 ; Pal.  Eureka  Dist.,  Mon.  U.  S.  Geol.  Survey,  vol.  8,  p. 

89,  pi.  9,  fig.  19.  Cambrian. 

finalis  Walcott,  1884;  Pal.  Eureka  Dist.,  Mon.  U.  S.  Geol.  Survey,  vol.  8,  p.  89, 

pi.  12,  figs.  12  a,b.  Pogonip. 

flabellifer  Hall  and  Whitfield,  1877;  U.  S.  Geol.  Expl.  40th  Par.,  vol.  4,  p.  227, 

pi.  2,  figs.  29, 30.  Potsdam. 

flagricaudus  White.  (See  Olenoides?  flagricauda.) 

? gothicus  Hall  and  Whitfield.  (See  Dorypyge  gothicus.) 

hisingeri  Billings,  1865;  Pal.  Foss.,  vol.  1,  p.  196,  fig.  182.  Quebec. 

inexpectans  Walcott,  1884  ; Pal.  Eureka  Dist.,  Mon.  U.  S.  Geol.  Survey,  vol.  8, 

p.  90,  pi.  1,  fig.  10.  Pogonip. 

? iowensis  Owen.  (See  Crepicephalus  iowensis  (Owen)  Walcott.) 

iole  Walcott,  1884 ; Pal.  Eureka  Dist.,  Mon.  U.  S.  Geol.  Survey,  vol.  8,  p.  43, 

pi.  10,  fig.  19.  Cambrian. 

latifrons  Shumard,  1863;  Trans.  Acad.  Sci.  St.  Louis,  vol.  2,  p.  101.  Potsdam. 

lodensis  Whitfield,  1880;  Ann.  Rept.  Geol.  Survey  Wisconsin,  1879,  p.  51. 

Potsdam. 

lodensis  Whitfield,  1882;  Geol.  Wisconsin,  vol.  4,  p.  188,  pi.  10,  fig.  14 ; p.  341, 

pi.  27,  figs.  12, 13. 

magnificus  Billings,  i860 ; Canadian  Naturalist,  vol.  5,  p.  307,  fig.  5 ( Bemoplcn - 

rides  magnificus  Billings,  1865;  Pal.  Foss.,  vol.  1,  p.  294).  Quebec. 

magnificus  Billings,  1865 ; Pal.  Foss.,  vol.  1,  p.  399,  fig.  376. 

? marcoui  Whitfield,  1884 ; Bull.  Am.  Mus.  Nat.  Hist.  New  York,  vol.  1,  p.  150, 

pi.  14,  fig.  7.  Potsdam. 

Referred  to  Olenoides  marcoui  Walcott,  1886;  Bull.  U.  S.  Geol.  Survey,  No.  30, 
p.  186,  pi.  26,  figs.  5, 5 a,  b. 

marica  Walcott,  1884;  Pal.  Eureka  Dist.,  Mon.  U.  S.  Geol.  Survey,  vol.  8,  p.  44, 

pi.  10,  fig.  13.  Cambrian. 

megalop  Billings,  1860  ; Canadian  Naturalist,  vol.  5,  p.  311,  fig.  9.  Quebec. 

megalop  Billings,  1865;  Pal.  Foss.,  vol.  1,  p.  403,  fig.  380. 

mini8caensi8.  (See  Ptychaspis  miniscaensis.) 

minnesotensis  Owen.  Cambrian. 

A very  large  sp.  Asaphus  Owen,  1848;  Rept.  Geol.  Reconnoissance  Chippewa 
Land  Dis.,  p.  15,  pi.  7,  figs.  2, 3. 

minnesotensis  Owen,  1852;  Rept.  Geol.  Survey  Wisconsin,  Iowa,  and  Minne- 
sota, p.  574,  pi.  1,  figs.  2, 10;  pi.  10,  figs.  3,  6. 

minnesotensis  Hall,  1863;  16th  Rept.  New  York  State  Cab.  Nat.  Hist.,  p.  138, 

pi.  9,  figs.  5-10  ; pi.  10,  figs.  10-12 ; pi.  11,  figs.  1-4,  6. 

Bull.  63 8 


114 


A BIBLIOGRAPHY  OF  PALEOZOIC  CRUSTACEA. 


[BULL.  63. 


Bikeiocephalus  minnesotensis  var.  limbatus  Hall,  1863;  16th  Rept.  New  York 
State  Cab.  Nat.  Hist.,  p.  141,  pi.  9,  fig.  12. 

; minnesotensis  var.  Hall.  1863;  16th  Rept.  New  York  State  Cab.  Nat.  Hist.,  p. 

141,  pi.  9,  fig.  11;  pi.  10,  fig.  9. 

minnesotensis  Winchell,  1864  ; Am.  Jour.  Sci.,  2d  series,  vol.  37,  p.  229. 

minnesotensis  Whitfield,  1882;  Geol.  Wisconsin,  vol.  4,  p.  187,  pi.  3,  fig.  1. 

misa  Hall,  1863;  16th  Rept.  State  Cab.  Nat.  Hist.,  p.  144,  pi.  8,  fig.  15 ; pi.  10, 

figs.  4-8.  Potsdam. 

missisquoi  Billings,  1865;  Pal.  Foss.,  vol.  1,  p.  199.  Quebec. 

multicinctus  Hall  and  Whitfield,  1877 ; U.  S.  Geol.  Expl.  40th  Par.,  vol.  4,  p. 

226,  pi.  2,  fig.  37.  Potsdam. 

nasutus  Walcott,  1884 ; Pal.  Eureka  Dist.,  Mon.  U.  S.  Geol.  Survey,  vol.  8,  p.  40, 

pi.  10,  fig.  15.  Cambrian. 

osceola  Hall,  1863;  16th  Rept.  New  York  State  Cab.  Nat.  Hist.,  p.  146,  pi.  7, 

fig.  49 ; pi.  10,  fig.  18.  Potsdam. 

osceola  Walcott,  1884  ; Pal.  Eureka  Dist.,  Mon.  U.  S.  Geol.  Survey,  vol.  8,p.  40, 

pi.  9,  fig.  25. 

oweni  Billings,  1860;  Canadian  Naturalist,  vol.  5,  p.  310,  fig.  8.  Quebec. 

oweni  Billings,  1865;  Pal.  Foss.,  vol.  1,  p.  402,  fig.  379. 

pauper  Billings,  1865;  Pal.  Foss.,  vol.  1,  p.  200.  Quebec. 

pepinensis  Owen,  1852 ; Rept.  Geol.  Survey  Wisconsin,  Iowa,  and  Minnesota, 

p.  574,  pi.  1,  figs.  9,  9 a;  pi.  1 a,  fig.  7.  Potsdam. 

pepinensis  Hall,  1863 ; 16th  Rept.  New  York  State  Cab.  Nat.  Hist.,  p.  142,  pi. 9, 

figs.  1-4 ; pi.  10,  figs.  13-17.  (Expl.,  pi.  11,  fig.  2.  See  Dicellocephalus 
crassimarginatus. ) 

pepinensitf'Winchell,  1864 ; Am.  Jour.  Sci.,  2d  series,  vol.  37,  p.  229. 

planifrons  Billings,  1860;  Canadian  Naturalist,  vol.  5,  p.  309,  fig.  6.  Quebec. 

planifrons  Billings,  1865;  Pal.  Foss.,  vol.  1,  p.  401,  fig.  377. 

quadriceps.  (See  Dorypyge  quadriceps.) 

richmondensis  Walcott,  1884  ; Pal.  Eureka  Dist.,  Mon.  U.  S.  Geol.  Survey,  vol. 

8,  p.  41,  pi.  10,  fig.  7.  Cambrian. 

roemeri  Shumard,  1861 ; Am.  Jour.  Sci.,  2d  series,  vol.  32,  p.  220.  Potsdam. 

selectus  Billings,  1865;  Pal.  Foss.,  vol.  1,  p.  199.  Quebec. 

selectus  Billiugs,  1865;  Pal.  Foss.,  vol.  1,  p.  198.  (See  Ptychaspis  selectus.) 

spiniger  Hall,  1863;  16ih  Rept.  New  York  State  Cab.  Nat.  Hist.,  p.  143,  pi.  10, 

figs.  1, 2, 3(?).  Potsdam. 

wahsatchensis.  (See  Olenoides  wahsatchensis.) 

Dionide  Barrande,  1847  ; Neues  Jahrbuch  fur  Mineral.,  vol.  4,  p,  391. 

Type,  Dionide  formosa  Barrande. 

Syn.,  Dione  Barrande;  Notice  Prelim.  Sil.  Syst.  Boheme,  p.  33. 

Polytomurus  Corda,  1847  ; Prodr.,  p.  153. 

? perplexa  Billings,  1866 ; Catalogue  Sil.  Foss.  Anticosti,  p.  67. 

Dipleura  Green,  1832;  Mon.  Tril.  North  America,  p.  79.  (See  Homalonotus  de- 
kayi.) 

Discranurus  Conrad,  1841 ; 5th  Rept.  Pal.  Dept.  New  York  Geol.  Survey,  p.  48.  (See 
Acidaspis  liamata.) 

Dolichometopus  Angelin,  1854 ; Palseont.  Scand.,  p.  72. 

Type,  Dolichometopus  sveticus  Ang. 

? convexus  Billings,  1865;  Pal.  Foss.,  vol.  1, p.  269, fig. 253. 

? gibberrulus  Billings,  1865 ; Pal.  Foss.,  vol.  1,  p.  269,  fig.  254. 

? rarus  Billings,  1865 ; Pal.  Foss.,  vol.  1,  p.  352,  fig.  308. 

Dorypyge  Dames,  1684;  China  (Richthofen),  vol.  4,  p.  23. 

Type,  Dorypyge  richthofeui  Dames. 

[ Dihelocephalus ] cristatus  Billings,  1865 ; Pal.  Foss.,  vol.  1,  p.  404,  fig.  384. 

Cambrian, 


Quebec. 

Quebec. 

Quebec. 


VOGDES.  j 


LIST  OF  TRILOBITES. 


115 


Dorypyge  IDikeloccphalus  f]  gothicus  Hall  and  Whitfield,  1877 ; U.  S.  Geol.  Expl. 

40th  Par.,  vol.  4,  p.  242,  pi.  1,  fig.  36.  Potsdam. 

gothicus  Dames,  18^4;  China  (Richthofen),  vol.  4,p.  23. 

[Dicellocephalus  ?]  gothicus  Walcott,  1884;  Pal.  Eureka  Dist.,  Mon.  U.  S.  Geol. 

Survey,  vol.  8,  p.  45,  pi.  9,  fig.  24.  Referred  to 

[Olenoides ] gothicus  Walcott,  1886;  Bull.  U.  S.  Geol.  Survey,  vol.  30,  p.  187,  pi. 

29,  figs.  1, 1 a-c. 

[ Dikelocephalus ] quadriceps  Hall  and  Whitfield,  1877 ; U.  S.  Geol.  Expl.  40th 

Par.,  vol.  4,  p.  240,  pi.  1,  tigs.  37-40.  Cambriau. 

[ Dicellocephalus ] quadriceps  Walcott,  1884;  Pal.  Eureka  Dist.,  Mon.  U.  S.  Geol. 

Survey,  vol.  8,  p.  45,  pi.  9,  fig.  24. 

quadriceps  Dames,  1884;  China  (Richthofen),  vol.  4,p.  23.  Referred  to 

[ Olenoides~\  quadriceps  Walcott,  1886 ; Bull.  U.  S.  Geol.  Survey,  No.  30,  p.  187,  pi. 

29,  figs.  1, 1 a-c. 

Dysplanus  Burmeister,  1843;  Organization  of  Trilobites  (Ray  Soc.  ed.,p.  205). 

Type,  Dysplanus  centrotus  Dalman. 

Ellipsocephalus  Zenker,  1833;  Beitriige  Naturgeschichte  der  Urwelt,  p.  51. 

Type,  Ellipsocephalus  hoffi  Bronn. 

curtus  Whitfield,  1878;  Ann.  Rept.  Geol.  Wisconsin,  1877,  p.  58.  Potsdam. 

cjirtus  Whitfield,  1882;  Geol.  Wisconsin,  vol.  4,  p.  191,  pi.  1,  fig.  18. 

Eliptocephalus  Emmons,  1844;  Taconic  Syst.,  p.  21,  figs.  1-3. 

asaphoides.  (See  Olenellus  asaphoides  Emmons.) 

Embolimus  Rominger,  1887 ; Proc.  Acad.  Nat.  Sci.  Phila.,  p.  16.  (See  Zacanthoides 
Walcott.) 

rotundata.  (See  Bathyuriscus  howelli.) 

spinosa.  (See  Olenoides  spinosus.) 

Encrinurus  Emmricli,  1844;  Zur  Naturg.  Trilobiten,  p.  16. 

Type,  Encrinurus  punctatus  Briinnich. 

americanus  Vogde.s,  1886;  Des.  New  Crust.  Clinton  Group  Georgia,  p.  1. 

Clinton. 

americanus  Foerste,  1887 ; Bull.  Denison  Univ.,  vol.  2,  p.  102. 

deltoideus  Shumard,  1855;  Geol.  Missouri,  p.  198,  pi.  B,  fig.  10. 

Upper  Silurian- 

[ Cryplonymus ] deltoideus  Yogdes,  1878;  Mon.  Genera  Zethus,  etc.,  p.  21. 

deltoideus  Foerste,  1887 ; Bull.  Denison  Univ.,  vol.  2,  p.  102. 

egani  Miller,  1879;  Jour.  Cincinnati  .Soc.  Nat.  Hist.,  vol.  2,  p.  254,  pi.  15,  figs. 

1,  l a,  b.  Niagara. 

elegantulus  Billings,  1866  ; Catalogue  Sil.  Foss.  Anticosti,  p.  62. 

elegantulus  Foerste,  1887 ; Bull.  Denison  Univ.,  vol.  2,  p.  102. 

excedrensis  Saflord.  (See  Encrinurus  varicostatus  Walcott.) 

Syn.,  excedrensis  Safford,  1869;  Geol.  Tennessee,  p.  290. 

mirus  Billings,  1865;  Pal.  Foss.,  vol.  1,  p.  292,  fig.  282.  Quebec. 

[ Cryptonymus~\  mirus  Yogdes,  1878  ; Mon.  Genera  Zethus,  etc.,  p.  34. 

[Amphion]  multisegmentatus  Portlock,  1843;  Geol.  Londonderry,  etc.,  p.  291, 

pi.  3,  fig.  6. 

multisegmentatus  Salter ; Mem.  Geol.  Survey  United  Kingdom,  decade  7,  pi.  4. 

multisegmentatus  Billings,  1866;  Catalogue  Sil.  Foss.  Anticosti,  p.  61. 

[Cryptonymus]  multisegmentatus  Vogdes,  1878  ; Mon.  Genera  Zethus,  etc.,  p.  29. 

nereus  Hall,  1867 ; 20tli  Rept.  Now  York  State  Cab.  Nat.  Hist.,  p.  375,  pi.  21, 

fig.  15.  Niagara. 

nereus  Hall,  1870  ; 20th  Rept.  New  York  State  Cab.  Nat.  Hist.,  p.  425,  pi.  21, 

fig.  15. 

[ Cryptonymus ] nereus  Vogdes,  1878 ; Mon.  Genera  Zethus,  etc.,  p.  24,  pi.  3,  fig.  17. 

ornatus  Hall  and  Whitfield,  1875;  Pal.  Ohio,  vol.  2,  p.  154,  pi.  7,  fig.  16. 

Niagara. 

Syn.,  Cybele punctata  Hall,  1852 ; Pal.  New  York,  vol.  2,  p.  297,  pi.  A 66,  figs,  1 a-k. 


116 


A BIBLIOGRAPHY  OF  PALEOZOIC  CRUSTACEA. 


[BULL.  63. 


Encrinurus  [ Cryptonymus ] ornatus  Yogdes,  1878;  Mon.  Genera  Zethus,  etc.,  p.  23. 

ornatus  Foerste,  1887 ; Bull.  Denison  Univ.,  vol.  2,  p.  102. 

punctatus  (Briinnich)  Billings,  1866;  Catalogue  Sil.'Foss.  Anticosti,  p.  61. 

thresheri  Foerstfc,  1887 ; Bull.  Denison  Univ.,  vol.  2,  p.  101,  pi.  8,  fig.  26. 

Clinton. 

trentonensis  Walcott,  1877;  Advance  sheets  31st  Rept.  New  York  State  Mus. 

Nat.  Hist.,  p.  15.  Trenton. 

trentonensis  Walcott,  1879;  31st  Rept.  New  York  State  Mus.  Nat.  Hist.,  p. 

68. 

[ Cryptonymus ] trentonensis  Yogdes,  1878;  Mon.  Genera  Zethus,  etc.,  p.  28. 

varicostatus  Walcott,  1877 ; Advance  sheets  31st  Rept.  New  York  State  Mus^ 

Nat.  Hist.,  p.  16.  Trenton. 

varicostatus  Walcott,  1879  ; 31st  Rept.  New  York  State  Cab.  Nat.  Hist.,  p.  69. 

[Cryptonymus J varicostatus  Yogdes,  1878;  Mon.  Genera  Zethus,  etc., p.  27. 

varicostatus  Safford  and  Yogdes,  1889 ; Proc.  Acad.  Nat.  Sci.  Phila.,  p.  167, 

figure. 

[ Ceraurus ] vigilans  Hall,  1847  ; Pal.  New  York,  vol.  1,  p.  245,  pi.  65,  figs.  2a-2  h. 

Trenton. 

[ Ceraurus ] vigilans  Emmons,  1855;  Am.  Geology,  vol.  1,  pt.  2,  p.  217,  pi.  15, 

figs.  2 a-2  c. 

[ Cryptonymus ] vigilans  Vogdes,  1878;  Mon.  Genera  Zethus,  etc.,  p.  29,  pi.  2, 

figs.  2 a-2  h. 

Endymion  Billings,  1862;  Pal.  Foss.,  vol.  1,  p.  94.  Changed  by  author  to  Endy- 
mionia. 

Endymionia  Billings,  1865;  Pal.  Foss.,  vol.  1,  p.  281. 

meeki  Billings,  1862  ; Pal.  Foss.,  vol.  1,  pp.  94  and  281,  fig.  84.  Quebec. 

Griffithides  Portlock,  1843;  Geol.  Rept.  Londonderry,  etc.,  p.  310. 

Type,  Griffithides  longiceps  Portlock.' 

[ Phillipsia  ( Griffithides )]  bufo  Meek  and  Worthen,  1870;  Proc.  Acad.  Nat.  Sci. 

Phila.,  p.  52.  Keokuk. 

[Phillipsia  (Griffithides)]  bufo  Meek  and  Worthen,  1873;  Geol.  Survey  Illinois, 

vol.  5,  p.  528,  pi.  19,  fig.  5. 

bufo  Yogdes,  1887 ; Annals  New  York  Acad.  Sci.,  vol.  4,  p.  95,  pi.  3,  figs.  4, 5, 10. 

[ Proetus]  granulatus  Wetherby,  1881 ; Jour.  Cincinnati  Soc.  Nat.  Hist.,  vol.  4, 

p.  31,  pi.  2,  figs.  8,  8 a,  9,  9 a.  Chester. 

granulatus  Yogdes,  1887 ; Annals  New  York  Acad.  Sci.,  vol.  4,  p.  101. 

[ Phillipsia  (Griffithides lodiensis  Meek.  (See  Brachymetopsis  lodiensis.) 

[ Phillipsia  ( Griffithides )]  portlocki  Meek  and  Worthen,  1865;  Proc.  Acad.  Nat. 

Sci.  Phila.,  p.  268.  Keokuk. 

[ Phillipsia  (Griffithides)']  portlocki  Meek  and  Worthen,  1873  ; Geol.  Survey  Illi- 
nois, vol.  5,  p.  525,  pi.  19,  fig.  6. 

portlocki  Walcott,  1884;  Pal.  Eureka  Dist.,  Mon.  U.  S.  Geol.  Survey,  vol.  8,  p. 

266,  pi.  24,  figs.  4, 4 a,  b. 

portlocki  Yogdes,  1887 ; Annals  New  York  Acad.  Sci.,  vol.  4,  p.  93,  pi.  3,  fig.  9. 

[. Phillipsia  ( Griffithides ?)]  sangamonensis  Meek  and  Worthen,  1865;  Proc. 

Acad.  Nat.  Sci.  Phila.,  p.  270.  Coal  Measures. 

[ Phillipsia  (Griffithides  ?)]  sangamonensis  Meek  and  Worthen,  1873;  Geol.  Sur- 
vey Illinois,  vol.  5,  p.  615,  pi.  32,  fig.  4. 

[ Phillipsia  (Griffithides  ?)]  sangamonensis  White,  1883;  13th  Rept.  Dept.  Geol. 

Nat.  Hist.  Indiana,  p.  174,  pi.  39,  figs.  4,5.  . 

[ Phillipsia ] sangamonensis  Herrick,  1887 ; Bull.  Denison  Univ.,  vol.  2,  p.  61, 

pi.  5,  fig.  13. 

[ Griffithides ] sangamonensis  Vogdes,  1887  ; Annals  New  York  Acad.  Sci.,  vol.  4, 

p.  99,  pi.  3,  figs.  7, 8. 

[ Phillipsia  (Griffithides)]  scitula  Meek  and  Worthen,  1865;  Proc.  Acad.  Nat.  Sci. 

Phila. , p.  270.  Coal  Measures. 


vogdes.]  CATALOGUE  OF  TRILOBITES.  117 

Griffithides  [ Phillipsia  ( Griffithides )]  scitula  Meek  and  Wortlien,  1873;  Geol.  Survey 
Illinois,  vol.  5,  p.  612,  pi.  32,  fig.  3. 

[ Phillipsia  ( Griffithides )]  scitula  While,  1883;  13th  Ann.  Kept.  Dept.  Geol.  Nat. 

Hist.  Indiana,  1882,  p.  173,  pi.  39,  figs.  6-9. 

iPhillipsia]  scitula  Meek,  1872;  U.  S.  Geol.  Survey  Territories,  Final  Kept.  Ne- 
braska, p.  238,  pi.  6,  fig.  9. 

[ Phillipsia ] scitula  Herrick,  1887  ; Bull.  Denison  Univ.,  vol.  2,  p.  62. 

scitula  Vogdes,  1887;  Annals  New  York  Acarl.  Sci.,  vol.  4,  p.  97,  pi.  2,  figs. 

11-13. 

? sedaliensis  Vogdes,  1888;  Trans.  New  York  Acad.  Sci.,  vol.  7,  p.  249. 

. Waverlv. 

[Phcethonides  ?]  sedaliensis  Herrick,  1839  ; Bull.  Denison  Univ.,  vol.  3,  p.  57. 

Harpes  Goldfuss,  1839 ; Nova  Acta  Acad.  Loop.  Carol.,  vol.  19,  p.  358. 

Type,  H'arpes  ungula  Sternb. 

antiquatus  Billings,  1859  ; Canadian  Naturalist,  vol.  4,  p.  469,  fig.  38.  Ckazy. 


antiquatus  Billings,  1863 ; Geol.  Canada,  p.  133,  fig.  67. 

consuetus  Billings,  1866;  Catalogue  Sil.  Foss.  Anticosti,  p.  64. 

dentoni  Billings,  1863;  Canadian  Naturalist,  vol.  8,  p.  3(5,  figure.  Trenton. 

c^ntoni  Billings,  1865 ; Pal.  Foss.,  vol.  1,  p.  183,  fig.  166. 

ecanabise  Hall,  1851 ; Rept.  Geol.  Lake  Superior  Land  Dist.  (Foster  and  Whit- 
ney), pt.  2,  p.  211,  pi.  27,  fig.  2 a.  Trenton. 

granti  Billings,  1865 ; Pal.  Foss.,  vol.  1,  p.  326,  fig.  314. 

ottawensis  Billings,  1865  ; Pal.  Foss.,  vol.  1,  p.  182,  fig.  165.  Trenton. 

Harpides  Beyrich,  1846  ; Untersueh.  Trilohiten,  p.  34. 

atlanticus  Billings,  1865 ; Pal.  Foss.,  vol.  1,  p.  281,  fig.  267.  Quebec. 

concentricus  Billings,  1865  ; Pal.  Foss.,  vol.  1,  p.  282,  fig.  268.  Quebec. 

? desertus  Billings,  1865 ; Pal.  Foss.,  vol.  1,  p.  333,  fig.  321.  Quebec. 


Hausmannia  Hall,  1888;  Pal.  New  York,  vol.  7,  p.  xxxi.  (Subgenus,  see  Dalma- 
nites.) 

Hemicr upturns  Green,  1832;  Mon.  Tril.  N.  A.,  p.  20. 

clintoni.  (See  Calymene  clintoni  Vanuxem.) 

Holometopus  Angelin,  1854 ; Pakeont.  Scand.,  p.  58. 

Type,  Holometopus  aciculatus,  pi.  33,  fig.  5. 

angelini  Billings,  1862;  Pal.  Foss.,  vol.  l,p.  95,  fig.  85;  alsop.  281.  Quebec. 

Homalonotus  Koenig,  1820;  leones  Foss.  Sectiles,  p.  4. 

Type,  Homalonotus  lenighti  Koenig,  pi.  7,  fig.  85. 

Syn.,  Brongniartia  Eaton,  1832;  Geological  Text  Book,  p.  32,  pi.  2,  fig.  20  (in 
part). 

Dipleura  Green,  1832;  Mon.  Tril.  N.  A.,  p.  78;  Monthly  Am.  Jour.  Geology, 
p.  560. 

Trimerus  Green,  1832;  Mon.  Tril.  N.  A.,  p.  81 ; Monthly  Am.  Jour.  Geology^ 
p.  560. 

Plcesiacomia  Cord  a,  1847;  Prodr.,  p.  171. 

Brogniartia  Salter,  1865  ; Mon.  Brit.  Tril.,  p.  104  (subgenus). 

Burmei8ieria  Salter,  1865;  Mon.  Brit.  Tril.,  p.  105  (subgenus). 

Koenigia  Salter,  1865;  Mon.  Brit.  Tril.,  p.  104  (subgenus). 

[ Asaphus ] cornigerus  (Scblotlieim)  Brong.,  1822;  Crust.  Foss.,  p.  18,  pi.  4,  fig.  10 

(not  pi.  2,  fig.  1). 

[ Asaphus ] crypturus  Green,  1834;  Trans.  Geol.  So'c.  Pennsylvania,  vol.  1,  p.  37, 

pi.  4.  Devonian. 

[ Asaphus  ?]  crypturus  Green,  1835 ; Suppl.  Mon.  Tril.  N.  A.,  p.  18,  cast  41. 

Syn.,  Asaphus  ditmarsice  Honoyinan,  1879 ; Proc.  Nova  Scotia  Inst.,  vol.  5,  p.  18. 

[ A8aphu8?~\  crypturus  Honeyman,  1888;  Proc.  Nova  Scotia  lust.,  vol.  7,  pt.  1, 

p.  63. 

dawsoni  Hall,  1860;  Canadian  Naturalist,  vol.  5,  p.  155. 


Silurian. 


118 


A BIBLIOGRAPHY  OF  PALEOZOIC  CRUSTACEA. 


[BULL.  63. 


Homalonotus  dawsoni  Dawson,  1878;  Acadian  Geology  (3d  ed.),  p.  606,  fig.  214. 

[ Dipleura ] dekayi  Green,  1832 ; Mon.  Tril.  N.  A.,  p.  79,  casts  30, 31,  pi.  1,  figs.  8,  9. 

Hamilton. 

Syn.,  Nuttainia  sparsa  Eaton,  1832;  Geological  Text  Book,  p.  34. 

Nuttainia  sparsa  Green,  1832;  Mon.  Tril.  N.  A.,  p.  89,  cast  35. 

I Dipleura']  dekayi  Yanuxem,  1842;  Geol.  New  York,  3d  Geol.  Dist.,  p.  150, 

fig.  1. 

[Dipleura]  dekayi  Hall,  1843;  Geol.  New  York,  4th  Geol.  Dist.,p.  205,  fig.  1 

dekayi  Emmons,  1860  ; Manual  Geology,  pp.  146, 147,  figs.  134, 135. 

dekayi  Hall,  1861 ; Des.  New  Species  Foss,  p.  85. 

dekayi  Hall,  1862;  15th  Rept.  New  York  State  Cab.  Nat.  Hist.,p.  113. 

dekayi  Hall,  1877  ; Illus.  Devonian  Foss.  Crust.,  pis.  2-5. 

dekayi  Hall,  1888 ; Pal.  New  York,  vol.  7,  p.  7,  pi.  2,  figs.  1-12 ; pi.  3,  figs.  1-5; 

pi.  4,  figs.  1-7  ; pi.  5,  figs.  1-4. 

[Trimerus]  delphinocephalus  Green,  1832;  Monthly  Am.  Jour.  Geol.,  vol.  1,  p. 

559,  pi.  0,  fig.  1.  Niagara. 

[Trimerus]  delphinocephalus  Green,  1832;  Mon.  Tril.  N.  A.,  p.  82,  pi.  1,  fig.  1, 

.cast  32. 

[Trimerus]  delphinocephalus  Harlan,  1835;  Trans.  Geol.  Soc.  Pennsylvania, 

vol.  l,p.  105. 

Syn.,  Brongniartia  platycephala  Eaton,  1832;  Geol.  Text  Book,  p.  32,  pi.  2,  fig.  20. 
Brongniartia platycepliala  Green,  1832;  Mon.  Tril.  N.  A.,p.  91. 

Ogygies  latisima  Eaton,  183i  ; Am.  Jour.  Sci.,  1st  series,  vol.  21,  p.  136  (foot- 
note). 

delphinocephalus  Murchison,  1839  ; Sil.  Syst.,  p.  651,  pi. 7 Zns,  figs.  1 a,  1 b. 

Syn.,  Ahrendii  Roemer,  1843  ; Yerst.  Harzzebirges,  p.  39,  pi.  11,  fig.  5. 

delphinocephalus  Hall,  1843 ; Geol.  New  York,  4th  Geol.  Dist.,  p.  103,  fig.  34. 

delphinocephalus  Yerneuil,  Note  sur  la  parall61isme,  etc.,  p.  47. 

Syn.,  atlas  Castelnau,  1843;  Syst.  Sil.  de  PAm6r.,p.  20. 
giganteus  Castelnau,  1843 ; Syst.  Sil.  de  FAm6r. 
herculaneus  Castelnau,  1843;  idem. 

delphinocephalus  Hall,  1852 ; Pal.  New  York,  vol.  2,  p.  309,  pi.  68,  figs.  1-14. 

— — delphinocephalus  Salter,  1865  ; Mon.  Brit.  Tril.,  p.  113,  pi.  11,  figs.  1-10. 

delphinocephalus  Hall,  1883;  12th  Ann.  Rept.  Dept.  Geol.  Nat.  Hist.  Indiana, 

1882,  p.  332,  pi.  34,  figs.  17, 18. 

delphinocephalus  ? Hall,  1875  ; 28th  Rept.  New  York  State  Mus.  Nat.  Hist.,  pi. 

34,  figs.  17, 18. 

delphinocephalus  Hall,  1879 ; 28th  Rept.  New  York  State  Mus.  Nat.  Hist.,  p.  187, 

pi.  32,  figs.  17, 18. 

[Trimerus]  jacksoni  Green,  1837  ; Am.  Jour.  Sci.,  1st  series,  vol.  32,  p.  347. 

Devonian. 

major  Whitfield,  1885  ; Bull.  Am.  Mus . Nat.  Hist.,  vol.  1,  No.  6,  p.  193,  pi.  22. 

Oriskany. 

major  Hall,  1888  ; Pal.  New  York,  vol . 7,  p.  4,  pi.  5 a,  fig.  1.  * 

vanuxemi  Hall,  1859  ; Pal.  New  York,  vol.  3,  p.  352,  pi.  73,  figs.  9-14. 

Lower  Helderberg. 

vanuxemi  Hall,  1888;  Pal.  New  York,  vol.  7,  p.  11,  pi.  5 b,  figs.  1,2. 

Hopolichas  Dames,  1877;  Zeitschr.  Deutsch.  geol.  Gesell.,  1872,  p.  794. 

Type,  Licha8  ( Hopolichas ) tricuspidata  Beyricli. 

Illaenurus  Hall,  1863;  16th  Rept.  New  York  State  Cab.  Nat.  Hist.,  p.  176. 

Type,  Illcenurus  quadratus  Hall. 

convexus  Whitfield,  1878;  Ann.  Rept.  Geol.  Survey  Wisconsin,  1877,  p.  66. 

♦ Lower  Magnesian. 

convexus  Whitfield,  1882 ; Geol.  Wisconsin,  vol.  4,  p.  203,  pi.  4,  figs.  3-5. 

eurekensis  Walcott,  1884  ; Pal.  Eureka  Dist.,  Mon.  U.  S.  Geol.  Survey,  vol.  8,  p. 

97,  pi.  12,  figs.  4, 4 a.  Pogonip. 


V0GDE6.J 


CATALOGUE  OF  TRILOBITES. 


119 


Illaenurus  quadratus  Hall,  1863  ; 16tli  Kept.  New  York  State  Cab.  Nat.  Hist.,  p.  176, 
pi.  7,  figs.  52-57.  Potsdam. 

Illaenus  Dalman,  1826  ; Palraad.,  p.  50. 

Type,  Illcenus crassicauda,  Wahl.,  Nova  Acta  Soc.  Scient.  Upsal.,  vol.  8,  p.  8,  pi.  2, 
figs.  5, 6 (not  pi.  7,  figs.  5, 6,  Illcenus  esmarki ). 

Syn.,  Actinolobus  Eichwald,  1860. 

Alceste  Corda,  1847. 

Cryptonymus  Eichwald,  1825  (in  part),  not  Cryptonymus  Eichwald,  1840. 
Deucalion  Stochegloff,  1827. 

JEclillcenus  Salter,  1866  (subgenus). 

Hydrolcenus  Salter,  1866  (subgenus). 

U lamopsis  Salter,  1865  (subgenus). 

Octillcenus  Salter,  1866  (subgenus). 

Thaleops  Conrad,  1843. 

ambiguus  Foerste,  1885  ; Bull.  Denison  Univ.,  vol.  1,  p.  106,  pi.  14,  figs.  9 a,  b ; 

fig.  10  a,  b,  c ; fig.  11.  Clinton. 

ambiguus  Foerste,  1887  ; Bull.  Denison  Univ.,  vol.  2,  p.  94. 

ambiguus  Foerste,  1886;  15th  Ann.  Rept.  Geol.  Nat.  Hist.  Survey  Minnesota,  p. 

480,  fig.  3. 

americanus  Billings,  1859 ; Canadian  Naturalist,  vol.  4,  p.  371.  Trenton. 

americanus  Billings,  1865 ; Pal.  Foss.,  vol.  1,  p.  329,  fig.  316  a-d ; fig.  318. 

angusticollis  Billings,  1859  ; Canadian  Naturalist,  vol.  4,  p.  377,  fig.  10  a-d. 

Trenton. 

arcturus  Hall,  1847 ; Pal.  New  York,  vol.  1,  p.  23,  pi.  4 Ms,  fig.  12. 

Chazy  and  Trenton. 

arcturus  Emmons,  1855 ; Am.  Geology,  vol.  1,  pt.  2,  p.  235,  pi.  3,  fig.  12. 

arcturus  (Hall)  Billings,  1859  ; Canadian  Naturalist,  vol.  4,  p.  379. 

arcturus  Billings,  1865  ; Pal.  Foss.,  vol.  1,  p.  279,  fig.  265. 

armatus  Hall,  1867;  20th  Rept.  New  York  State  Cab.  Nat.  Hist.,  p.  330,  pi.  22, 

figs.  1.2.  Niagara. 

armatus  Hall,  1870  ; 20th  Rept.  New  York  State  Cab.  Nat.  Hist.,  p.  418,  pi.  22, 

figs.  1, 2 ; pi.  25,  fig.  22. 

armatus?  Hall,  1875  ; 28th  Rept.  New  York  State  Mus.  Nat.  Hist.,  pi.  32,  figs. 

19, 20. 

armatus?  Hall,  1879 ; 28th  Rept.  New  York  State  Mus.  Nat.  Hist.,  p.  189,  pi.  32, 

figs.  19, 20. 

armatus  Hall,  1883 ; 12th  Ann.  Rept.  Dept.  Geol.  Nat.  Hist.  Indiana,  1882,  p.  335, 

pi.  34,  figs.  19, 20  ; pi.  33,  fig.  12. 

barriensis  (Murch.)  Hall;  Trans.  Albany  Inst.,  vol.  4,  p.  227;  abstract,  p.  33, 

May,  1863. 

barriensis  (Murch.)  Roemer,  1860;  Die  sil.  Fauna  W.  Tennessee,  p.  83,  pi.  5, 

fig.  23.  Niagara. 

\_Bumastm']  barriensis  (Murch.),  1839;  Sil.  Syst.,  p.  656,  pi.  7 Ms,  figs.  3 a-d, 

pi.  14,  fig.  7 (in  part). 

barriensis  Salter,  1859 ; Murchison’s  Siluria  (2d.  ed.),  pi.  17,  figs.  9-11. 

bayfieldi  Billings,  1859 ; Canadian  Naturalist,  vol.  4,  p.  369,  figs.  4-6.  Chazy. 

clavifrons  Billings,  1$59  ; Canadian  Naturalist,  vol.  4,  p.  379. 

Chazy  and  Trenton. 

conifrons  Billings,  1859 ; Canadian  Naturalist,  vol.  4,  p.  378,  figs.  7-9.  Trenton. 

conradi  Billings,  1859;  Canadian  Naturalist,  vol.  4,  p.  372,  figs.  7-9.  (See  Pan- 

deria  conradi.)  Trenton. 

consimilis  Billings,  1865;  Pal.  Foss.,  vol.  1,  p.  277,  figs.  263  a-c ; p.  331,  fig.  317. 

Compare  Ilhenus  esmarki  Schlotheim.  Quebec. 

consobrinus  Billings,  1865;  Pal.  Foss.,  vol.  1,  p.  280,  fig.  268;  p.  332,  fig.  320. 

Quebec. 


[BULL.  63. 


120  A BIBLIOGRAPHY  OF  PALEOZOIC  CRUSTACEA. 

Illaenus  cornigerus  Hall,  1872;  24tli  Rept.  New  York  State  Cal).  Nat.  Hist.,  p.  186, 
pi.  13,  tigs.  20, 21.  Clinton. 

[j Entomo8tracetes~\  crassicauda  Wahlenberg,  1821;  Nova  Acta  Soc.  Scieut.  Upsal., 

vol.  8,  p.  27,  pi.  2,  figs.  5, 6 (not  pi.  7,  figs.  5, 6). 

crassicauda  Holm,  1882;  Svenska  Vet.-Akad.  Handl.,  vol.  7,  No.  3,  pi.  2, 

figs.  21-27. 

crassicauda  ? Hall,  1847 ; Pal.  New  York,  vol.  1,  p.  24,  pi.  4 bis,  fig.  13;  pi.  60, 

figs.  4 a-d. 

crassicauda  (Wahl.)  Meek  and  Wortken,  Geol.  Survey  Illinois,  vol.  3,  p.  322, 

pi.  3,  figs.  1 a-1  b. 

Compare  Illcenus  consimilis  and  I.  esmarckii. 

cuniculus  Hall,  1867 ; 20th  Rept.  New  York  State  Cab.  Nat.  Hist.,  p.  377,  pi.  22, 

fig.  12.  Niagara. 

cuniculus  Hall,  1870  ; 20th  Rept.  New  York  State  Cab.  Nat.  Hist.,  p.  421,  pi.  22, 

fig.  12  (rev.  ed.). 

daytonensis  Hall  and  Whitfield,  1875 ; Pal.  Ohio,  vol.  2,  p.  119,  pi.  5,  figs.  14-16. 

Ciinton. 

daytonensis  Foerste,  1885;  Bull.  Denison  Univ.,  vol.  1,  p.  104,  pi.  14,  figs.  4 a, 

b ; figs.  6,  7,  7 a,  b,  c. 

daytonensis  Foerste,  1887;  Bull.  Denison  Univ.,  vol.  2,  p.  93,  pi.  8,  figs.  1-7. 

fraternus  Billings,  1865;  Pal.  Foss.,  vol.  1,  p.  276,  figs.  262  a,  b.  Quebec. 

globosus  Billings,  1859 ; Canadian  Naturalist,  vol.  4,  p.  367,  figs.  1-3.  Cliazy. 

[ Bumastus ] graftonensis  Meek  and  Worthen,  1870;  Proc.  Acad.  Nat.  Sci.Phila., 

p.  54. 

[Rumasfus]  graftonensis  Meek  and  Worthen,  1875;  Geol.  Survey  Illinois,  vol. 

6,  p.  508,  pi.  25,  fig.  4. 

grandis  Billings,  1859  ; Canadian  Naturalist,  vol.  4,  p.  380.  Hudson  River. 

— — herricki  Foerste,  1886;  15th  Ann.  Rept.  Geol.  Nat.  Hist.  Minnesota,  p.  479, 
* fig.  2.  Trenton. 

imperator  Hall,  1861 ; Rept.  Progress  Geol.  Survey  Wisconsin,  p.  49.  Niagara. 

imperator  Hall,  1867  ; 20th  Rept.  New  York  State  Cab.  Nat.  Hist.,  p.  332,  pi.  22, 

figs.  15-17;  pi.  2.3,  figs.  2: 3. 

imperator  Hall,  1870;  20th  Rept.  New  York  State  Cab.  Nat*  Hist.,  p.  420,  pi. 

22,  figs.  15-17 ; pi.  23,  figs.  2,  3. 

imperator  Whitfield,  1882;  Geol.  Wisconsin,  vol.  4,  p.  306,  pi.  21,  figs.  4,5. 

incertus  Billings,  1865;  Pal.  Foss.,  vol.  1.  p.  332,  fig.  319.  Quebec. 

* indeterminatus  Walcott,  1877 ; Advanced  sheets  31st  Rept.  New  York  State 

Mus.  Nat.  Hist.,p.  19.  Trenton. 

indeterminatus  Walcott,  1879 ; 31st  Rept.  New  York  State  Mus.  Nat.  Hist.,  p.  70. 

insignia  Hall,  1867  ; 20th  Rept.  New  York  State  Cab.  Nat.  Hist.,  p.  331,  figs.  5, 

6,  pi.  22,  figs.  13,  14. 

[ Bumastus ] insignis  Salter,  1867 ; Mon.  Brit.  Tril.,  p.  207. 

insignis  Hall,  1867  ; 20th  Rept.  New  York  State  Ca"b.  Nat.  Hist.,  p.  331,  figs.  5, 6; 

pi.  22,  figs.  13, 14. 

insignis  Hall,  1870;  20th  Rept.  New  York  State  Cab.  Nat.  Hist.;  p.  419,  figs.  10, 

11 ; pi.  22,  figs.  13, 14. 

[ Bumastus ] insignis  Meek,  1873  ; Pal.  Ohio,  vol.  1,  jh  189,  pi.  15,  figs.  5 a-c. 

insignis  Holm,  1882;  De  Svenska  Art.  Tril.  Illsenus,  p.  127. 

insignis  Whitfield,  1882 ; Geol.  Wisconsis,  vol.  4,  p.  305,  pi.  21,  figs.  6-10. 

insignis  Foerste,  1886;  15th  Ann.  Rept.  Geol.  Nat.  Hist.  Survey  Minnesota',  p. 

481. 

ioxus  Hall,  1867  ; 20tli  Rept.  New  York  State  Cab.  Nat.  Hist.,  p.  378,  pi.  22,  figs. 

4-10.  Niagara. 

IBumastus']  ioxus  Hall,  1870;  20th  Rept.  New  York  State  Cab.  Nat.  Hist.,  p. 

420,  pi.  22,  figs.  4-10. 


VOGDES.J 


CATALOGUE  OF  TRILOBITES. 


121 


Illaenus  [ Bumastus ] ioxus  Hall,  1883;  12tli  Ann.  Rept.  Dept.  Geol.  Nat.  Hist.  In- 
diana, 1882,  p.  335,  pi.  38,  figs.  13, 14. 

ioxus  Whitfield,  1882;  Geol.  Wisconsin,  vol.  4,  p.  304,  pi.  21,  figs.  11, 12. 

[ Bumastus ] ioxus  Hall,  1883  ; Trans.  Albany  Inst.,  vol.  10,  p.  76. 

latidorsata  Hall,  1847 ; Pal.  New  York,  vol.  1,  p.  230,  pi.  60,  figs.  6 a,  b.  Trenton. 

madisonianus  Whitfield,  1882;  Geol.  Wisconsin,  vol.  4,  p.  307,  pi.  20,  figs.  8,9. 

Niagara. 

madisonianus  Foerste,  1885;  Bull.  Denison  Univ.,  vol.  1,  p.  106,  pi.  14,  figs.  1 

a,  b and  2 a,  b. 

madisonianus  Foerste,  1887  ; Bull.  Denison  Univ.,  vol.  2,  p.  93,  pi.  8,  figs.  8-10. 

Clinton. 

milleri  Billings,  1859;  Canadian  Naturalist,  vol.  4,  p.  375,  fig.  10.  Trenton. 

milleri  Walcott,  1877 ; Advance  sheets  31st  Rept.  N.  Y.  State  Mus.  Nat.  Hist., 

p.  20. 

milleri  Walcott,  1879 ; 31st  Rept.  N.  Y.  State  Mus.  Nat.  Hist.,  p.  71. 

[A7iZews]  minnesotensis  Foerste,  1886  ; 15th  Ann.  Rept.  Geol.  Minnesota,  p.  478, 

fig.  1.  Trenton.  • 

niagarensis  Whitfield,  1880 ; Ann.  Rept.  Geol.  Wisconsin,  1879,  p.  69.  Niagara. 

Name  changed,  by  request  of  the  Wisconsin  Geological  Survey,  from  Illcenus 
niagarensis  to  Illaenus  madisonianus.  Explanation  omitted  by  accident  in 
the  Final  Report  Pal.  Wisconsin,  p.  307. 

orbicaudatus  Billings,  1859;  Canadian  Naturalist,  vol.  4,  p.  379.  Hudson. 

[ Thaleops ] ovatus  Conrad,  1843;  Proc.  Acad.  Nat.  Sci.  Phila.,  vol.  1,  p.  332. 

Trenton. 

[ Tlialeops  (Illcenus)]  ovatus  Hall,  1847 ; Pal.  New  York,  vol.  1,  p.  259,  pi.  67,  figs- 

6 a-b. 

ovatus  Whitfield,  1882 ; Geol.  Wisconsin,  vol.  4,  p.  238,  pi.  5,  figs.  1, 2. 

pomatia  Salter,  1867 ; Mon.  Brit.  Tril.,  pi.  27,  figs.  6, 7. 

pterocephalus  Whitfield,  1878  ; Ann.  Rept.  Geol.  Wisconsin,  1877,  p.  87. 

Niagara. 

pterocephalus  Whitfield,  1882 ; Geol.  Wisconsin,  vol.  4,  p.  309,  pi.  20,  figs.  10-12. 

simulator  Billings,  1865 ; Pal.  Foss.,  vol.  1,  p.  337,  figs.  315  a,  b.  Quebec. 

taurus  Hall,  1861 ; Rept.  Prog.  Geol.  Survey  Wisconsin,  p.  49.  Niagara. 

taurus  Meek  and  Worthen,  1865 ; Geol.  Survey  Illinois,  vol.  3,  p.  320,  pi.  3,  fig.  2. 

[ Bumastus ] trentonensis  Emmons,  1842  ; Geol.  New  York,  3d  Geol.  Dist.,p.  390 

fig.  1.  Trenton. 

[Bumastus]  trentonensis,  1854  ; 7th  Rept.  New  York  State  Cab.  Nat.  Hist.,  p.  64, 

fig.  1. 

[ Bumastus ] trentonensis  Emmons,  1855;  Am.  Geology,  vol.  1,  pt.  2,  p.  215,  pi.  15, 

fig.  13. 

trentonensis  Hall,  1847  ; Pal.  New  York,  vol.  1,  p.  230,  pi.  60,  fig.  5. 

tumidifrons  Billings,  1865  ; Pal.  Foss.,  vol.  1,  p.  278,  fig.  264.  Quebec. 

vindex  Billiugs,  1865 ; Pal.  Foss.,  vol.  1,  p.  179,  fig.  160.  Cliazy. 

[Bumastus]  worthenanus  Winchell  and  Marcy,  1866;  Mem.  Boston  Soc.  Nat. 

Hist.,  vol.  1,  pt.  1,  p.  105,  pi.  3,  fig.  13  (referred  by  Hall,  20th  Rept.  New  York 
State  Cab.  Nat.  Hist.,  to  Illcenus  armatus  Hall). 
l8oletu8  De  Kay,  1825;  Annals  Lyceum  Nat.  Hist.  New  York,  vol.  1,  p.  174. 

canalis.  (See  Asaphus  canalis.) 

cgclop8.  (See  Asaphus  platycephalus.) 

gigas.  (See  Asaphus  platycephalus.) 

maximu8.  (See  Asaphus  maximus.) 

megalops  Green,  1832;  Mon.  Tril.  N.  A.,  p.  70,  cast  7b. 

megistos.  (See  Asaphus  maximus.) 

platycephalus.  (See  Asaphus  platycephalus.)  • 

planus.  (See  Asaphus  platycephalus.) 


122 


A BIBLIOGRAPHY  OF  PALEOZOIC  CRUSTACEA. 


[bull.  63. 


Isolelus  stegops.  (See  Asaphus  platycephalus. ) 

vigilans,  (See  Asaphus  vigilans.) 

Lichas  Dalman,  1826;  Palsead.,  pp.  53, 71,  pi.  6,  fig.  1. 

Type,  Lichas  laciniatus  Wahlenberg. 

Syn.,  Platynotus  Conrad,  1838;  Geol.  Survey  New  York,  Rept.  Pal.  Dept.,  p.  118. 
Arges  Goldfuss,  1839  (in  part). 

Metopias  Eichwald,  1842 ; Die  Urwelt  Russ.,  p.  62,  pi.  3,  figs.  21-23. 
Actinurus  Castelnau,  1843;  Syst.  Sil.  de  FAm6r.,p.  21. 

Nuttainia  Portlock  and  Emrurich. 

Corydocephalus  Corda,  1847  ; Prodr.,  p.  255. 

Dicranopeltis  Corda,  1847  ; Prodr.,  p.  257. 

Acanthopyge  Corda,  1847 ; Prodr.,  p.  260. 

Dicranoymas  Corda,  1847;  Prodr.,  p.  261. 

Subgenera,  Hoplolichas  Dames,  1877;  Zeitscbr.  Deutsch.  geol.  Gesellsch.,  1877,  p. 
794. 

Type,  Hoplolichas  tricuspidata  Beyrich. 

Conolichas  Dames,  1877;  Zeitschr.  Deutscli.  geol.  Gesellsch.,  1877,  p.  806. 
Type,  Conolichas  cequiloha  Steinhardt. 

armatus  Hall.  (See  Acidaspis  eriopis  Hall.) 

bigsbyi  Hall,  1859 ; Pal.  New  York,  vol.  3,  p.  364,  pi.  77,  figs.  1-8. 

Lower  Helderberg. 

1 Conolichas']  bigsbyi  ? Hall,  1888 ; Pal.  New  York,  vol.  7,  p.  80,  pi.  19  a,  fig.  1. 

[ Paradoxides ] boltoni  Bigsby,  1825;  Jour.  Acad.  Nat.  Sci.  Phila.,  vol.  4,  p.  365, 

plate.  Niagara. 

[ Paradoxides ] boltoni  Green,  1832  ; Monthly  Am.  Jour.  Geol.,  etc.,  vol.  1,  p.  560, 

pi.  1,  fig.  5. 

[ Paradoxides ] boltoni  Green,  1832;  Mon.  Tril.  North  America,  p.  60,  pi.  1,  fig.  5. 

[ Paradoxides ] boltoni  Harlan,  1834 ; Trans.  Geol.  Soc.  Penn.,  vol.  1,  p.  103. 

[ Paradoxides ] boltoni  Harlan,  1835;  Med.  and  Phys.  Researches,  p.  303. 

\_Plaiynotus]  boltoni  Conrad,  1838 ; Rept.  Pal.  Dept.  Geol.  Survey  New  York, 

p.  118. 

[ Actinurus]  boltoni  Castelnau,  1843  ; Syst.  Sil.  de  TAm6r.,  p.  21,  pi.  3,  fig.  3. 

boltoni  Hall,  1852 ; Pal.  New  York,  vol.  2,  p.  311,  pi.  69  ; pi.  70,  figs.  1 a-i. 

boltoni  Meek  and  Worthen,  1875;  Geol.  Survey  Illinois,  vol.  6,  p.  508,  pi.  25, 

fig.  5. 

boltoni  var.  occidentalis  Hall,  1863;  Trans.  Albany  Inst.,  vol.  4,  p.  223;  ab- 
stract, p.  29. 

boltoni  var.  occidentalis  Hall,  1875 ; 28th  Rept.  New  York  State  Mus.  Nat. 

Hist.  Expl.,  p.  34,  figs.  8-11. 

boltoni  var.  occidentalis  Hall,  1879;  28tli  Rept.  New  York  State  Mus.  Nat. 

Hist.,  p.  198,  pi.  34,  figs.  8-11. 

boltoni  var.  occidentalis  Hall,  1883 ; 12th  Ann.  Rept.  Dept.  Geol.  Nat.  Hist. 

Indiana,  1882,  p.  334,  pi.  36,  figs.  8,  11, 12  (?). 

breviceps  Hall,  1863 ; Trans.  Albany  Inst.,  vol.  4,  p.  222;  abstract,  p.  28. 

Niagara. 

breviceps  Hall  and  Whitfield,  1875 ; Pal.  Ohio,  vol.  2,  p.  156,  pi.  6,  fig.  17. 

breviceps  Hall,  1875;  28th  Rept.  New  York  State  Mus.  Nat.  Hist.  Expl.,  pi.  34, 

figs.  1-7. 

breviceps  Hall,  1879 ; 28th  Rept.  New  York  State  Mus.  Nat.  Hist.,  p.  197,  pi.  34, 

figs.  1-7. 

breviceps  Hall,  1883;  12th  Ann.  Rept.  Dept.  Geol.  Nat.  Hist.  Indiana,  1882,  p. 

343,  pi.  36,  figs.  1-7. 

breviceps  Foerste,  1885 ; Bull.  Denison  Univ.,  vol.  1,  p.  112,  pi.  13,  figs.  2, 6 a,  b. 

Clinton. 


vogdesI  CATALOGUE  OF  TRILOBITES.  123 

Liclias  breviceps  Foerste,  1837  ; Bull.  Denison  Univ.,  vol.  2,  p.  98,  pi.  8,  figs.  18, 19. 
Not  Lichas  breviceps  Hall,  1867  ; 20tli  Rept.  New  York  State  Cab.  Nat.  Hist.,  p. 
377,  pi.  21,  figs.  12-14;  also  rev.  ed.,  p.  424,  pi.  21,  figs.  12-14.  (See  Liclias 
emarginatus.) 

canadensis  Billings,  1866;  Catalogue  Sil.  Foss.  Anticosti,  p.  65,  fig.  22. 

champlainensis  Whitfield,  1886;  Bull.  Am.  Mus.  Nat.  Hist.  New  York,  vol.  1,  No. 

8,  p.  342,  pi.  23,  figs.  6-8.  Birdseye. 

[ Arges ] contusus  Hall,  1888  ; Pal.  New  York,  vol.  7,  p.  83,  pi.  19  b,  figs.  3-6. 

Upper  Helderberg. 

cucullus  Meek  and  Worthen,  1865 ; Proc.  Acad.  Nat.  Sci.  Phila.,  p.  266. 

Trenton. 

cucullus  Meek  and  Worthen,  1866;  Geol.  Survey  Illinois,  vol.  3,  p.  299,  pi.  1, 

figs.  6 a-c. 

decipiens  Winchell  and  Marcy,  1866;  Mem.  Boston  Soc.  Nat.  Hist.,  vol.  l,pt.  1, 

p.  104,  pi.  3,  fig.  11.  Niagara. 

[ Ceratolichas ] dracon  Hall,  1888  ; Pal.  New  York,  vol.  7,  p.  85,  pi.  19,  figs.  14-17. 

Hall,  1876;  Ulus.  Devonian  Foss.  Crust.,  pi.  19,  figs.  2, 3.  Upper  Helderberg. 

emarginatus  Hall,  1879;  28th  Rept.  New  York  State  Mus.  Nat.  Hist.,  p.  199. 

.Niagara. 

Syn.,  Lichas  breviceps  Hall;  20th  Rept.  New  York  State  Cab.  Nat.  Hist.,  p.  377, 
pi.  21,  figs.  12-14,  rev.  ed.,  p.  424,  pi.  21,  figs.  12-14. 

eriopis,  Hall.  Upper  Helderberg. 

Syn.,  Lichas  armatus  Hall,  1861 ; Des.  New  Species  Foss.,  p.  81. 

Liclias  armatus  Hall,  1862;  15th  Rept.  New  York  State  Cab.  Nat.  Hist.,  p. 
109. 

eriops  Hall,  1863;  16th  Rept.  New  York  State  Cab.  Nat.  Hist.,  p.  226. 

[ Acidaspis  ( Terataspis )]  eriops  Hall,  1876;  Illus.  Devonian  Foss.  Crust.,  pi.  19, 

figs.  4-7,10, 11. 

[ Acidaspis  (Terataspis?)  ] sp.  ? Hall,  1876;  Illus.  Devonian  Foss.  Crust.,  pi.  19, 

fig.  12. 

[ Conolichas ] eriops  Hall,  1888;  Pal.  New  York,  vol.  7,  p.  78,  pi.  19  a,  figs.  2-13, 

15, 16. 

grandis  Hall,  1861 ; Des.  New  Species  Foss.,  p.  82.  Upper  Helderberg. 

grandis  HalJ,  1862;  15th  Rept.  New  York  State  Cab.  Nat.  Hist.,  p.  110. 

grandis  Hall,  1863  ; 16th  Rept.  New  York  State  Cab.  Nat.  Hist.,  i>.  223.  (Sub- 
genus Terataspis.) 

Syn.,  superbus  Billings,  1875;  Canadian  Naturalist,  vol.  7,  p.  239. 

[ Acidaspis  ( Terataspis )]  grandis  Hall,  1876;  Illus.  Devonian  Foss.  Crust.,  pis. 

17, 18. 

[Terataspis]  grandis  Hall,  1888;  Pal.  New  York,  vol.  7,  p.  73,  pi.  17,  figs.  1-6; 

pi.  1*,  figs.  1,2;  pi.  19,  figs.  1-7. 

[ Ceratolichas ] grandis  Hall,  1888;  Pal.  New  York,  vol.  7,  p.  84,  pi.  19  b,  figs. 

7-13. 

[ Ceratolichas ] gryps  Hall,  1888;  Pal.  New  York,  vol.  7,  p.  84,  pi.  19  b,  figs. 

7-13. 

harrisi  Miller,  1878;  Jour.  Cincinnati  Soc.  Nat.  Hist.,  vol.  1,  p.  106,  pi.  3,  fig.  9. 

Hudson. 

[ Acidaspis  n.  sp.  ?]  Hall,  1876;  Illus.  Devonian  Foss.  Crust.,  pi.  19,  fig.  1 (not  figs. 

2,3).  Upper  Helderberg. 

[ Conolichas ] hispidus  Hall,  1888;  Pal.  New  York,  vol.  7,  p.  77,  pi.  19  a,  ligs.  14, 

17,  18. 

Syn.,  [ Acidaspis  ( Terataspis )]  eriops  Hall,  1876;  Illus.  Dev.  Foss.,  pi.  19,  figs.  8,9. 

Upper  Helderberg. 

[Hoplolichas]  hylaeus  Hall,  1888;  Pal.  New  York,  vol.  7,  p.  81,  pi.  19  b,  ligs.  1,2. 

Upper  Helderberg. 

jukesi  I3i lliugs,  1865;  Pal.  Foss.,  vol.  1,  p.  282,  fig.  260;  also  p.  335,  fig.  323. 

Quebec. 


124 


A BIBLIOGRAPHY  OF  PALEOZOIC  CRUSTACEA. 


[bull.  63. 


Lichas  minganensis  Billings,  1865;  Pal.  Foss.,  vol.  1,  p.  181,  figs.  163  a,  b. 

Chazy  and  Trenton. 

nereus  Hall,  1863;  16th  Rept.  New  York  State  Cab.  Nat.  Hist.,  p.  226. 

Niagara. 

obvius  Hall,  1870;  20th  Rept.  New  York  State  Cab.  Nat.  Hist.,  p.  424,  pi.  25, 

fig.  19-  Niagara. 

[ Calymene]  phlyctanodes  Green,  1837  ; Am.  Jour.  Sci.,  1st  series,  vol.  32,  p.  167. ' 

Niagara. 

[Arges]  phlyctanodes  Hall,  1852;  Pal.  New  York,  vol.  2,  p.  314,  pi.  70,  figs. 

2 a,  c. 

[ Dicranogmus]  ptyonurus  Hall,  1888 ; Pal.  New  York,  vol.  7,  p.  86,  pi.  19  b,  figs. 

19-21.  Niagara. 

pugnax  Winchell  and  Marcy,  1866 ; Mem.  Boston  Soc.  Nat.  Hist.,  vol.  1,  pt.  1, 

p.  103,  pi.  3,  fig.  10.  Niagara. 

pugnax  Hall,  1867  ; 20th  Rept.  New  York  State  Cab.  Nat.  Hist.,  p.  393  (rev.  ed., 

p.  424,  pi.  25,  tig.  20). 

pustulosus  Hall,  1859 ; Pal.  New  York,  vol.  3,  p.  366,  pi.  77,  figs.  9-12 ; pi.  78, 

figs.  1-6,  fig.  7 (T).  Lower  Helderberg. 

puhtulosus  Hall,  1876 ; Illus.  Devonian  Foss.  Crust.,  pi.  19,  fig.  13. 

[Conoliclias]  pustulosus  Hall,  1888;  Pal.  New  York,  vol.  7,  p.  80,  pi.  19,  figs. 

8,  10,  11. 

superbus  Billings,  1875;  Canadian  Naturalist,  n.  s:,  vol.  7,  p.  239.  (See  Lichas 

grandis.)  Corniferous. 

[ Asaphus? ] trentonensis  Conrad,  1842;  Jour.  Acad.  Nat.  Sci.  Phila.,  vol.  8,  p. 

277,  pi.  16,  fig.  16.  Trenton. 

[ Platynotus ] trentonensis  Hall,  1847  ; Pal.  New  York,  vol.  1,  p.  235,  pi.  64,  figs. 

1 a-e. 

— - trentonensis  Miller,  1874  ; Cincinnati  Quart.  Jour.  Sci.,  vol.  1,  p.  127. 

Lloydia  Vogdes,  1889  (generic  name  for  Bathyurus  bituberculatus  Billings  for  its  type). 
Loganellus  Devine,  1863 ; Canadian  Naturalist,  vol.  8,  p.  95.  (See  Ptychoparia, 
Crepicephalus,  and  Olenus.) 

logani  Devine,  1863;  Canadian  Naturalist,  vol.  8,  p.  95.  (See  Ptychoparia 

logani.) 

[Olenus?]  logani  Billings,  1865;  Pal.  Foss.,  vol.  1,  p.  201,  figs.  185, 186. 

quebecensis  Billings,  1865 ; Pal.  Foss.,  vol.  1,  p.  203.  (See Ptychoparia  logani.) 

Lonchocephalus  Owen,  1852;  Rept.  Geol.  Survey  Wisconsin,  Iowa,  and  Minnesota, 
p.  576.  (See  Anomocare  hamulus  (Owen)  Dames.) 

Megalaspis  Angelin,  1852;  Palseont.  Scand.,  p.  15. 

Type,  Megalaspis  gigas  Ang.,  pi.  12,  fig.  3. 

belemnurus  White,  1874  ; Rept  .Invert.  Foss.,  etc.,  p.  11.  Quebec. 

belemnurus  White,  1877;  Geog.  Sur.  W.  100th  Meridian,  Pal.,  vol.  4,  p.  59, 

pi.  3,  fig.  9. 

[Asaphus  ( meglaspis )]  goniocerus  Meek,  1873;  6th  Ann.  Rept.  Geol.  Survey 

Territories,  1872,  p.  480.  Quebec. 

Menocephalus  Owen,  1852)  Rept.  Geol.  Survey  Wisconsin,  Iowa,  and  Minnesota, 
p.  577. 

Dr.  D.  D.  Owen  refers  one  species  to  this  genus,  Menocephalus  mimiesotensis, 
pi.  1,  fig.  11,  which  has  a highly  arched  and  hemispherical  glabella. 

globosus  Billings,  1860 ; Canadian  Naturalist,  vol.  5,  p.  317,  figs.  17-19. 

Quebec. 

globosus  Billings,  1865 ; Pal.  Foss.,  vol.  1,  p.  408,  figs.  388  a-c. 

minnesotensis  Owen,  1852 ; Rept.  Geol.  Survey  Wisconsin,  Iowa,  and  Minne- 
sota,^. 577,  pi.  1,  fig.  11.  Cambrian. 

salteri  Billings,  1863;  Canadian  Naturalist,  vol.  8,  p.  210,  figure.  Cambrian. 

salteri  Billings,  1865;  Pal.  Foss.,  vol.  1,  p.  203,  fig.  187. 


vogdes.]  CATALOGUE  OF  TRILOBITES.  125 

Menocephalus  salteri  ? Rominger,  1888;  Proc.  Acad.  Nat.  Sci.  Phila.,  pi.  16,  pi.  1, 
fig.  6. 

sedgwicki  Billings,  1860 ; Canadian  Naturalist,  vol.  5,  p.  316,  fig.  16.  Quebec. 

sedgwicki  Billings,  1865 ; Pal.  Foss.,  vol.  1,  p.  407,  fig.  387. 

Mesonacis  Walcott,  1885;  Am.  Jour.  Sci.,  3d  series,  vol.  29,  p.  329. 

\_Olenu.8~\  vermontana  Hall,  1859;  12th  Rept.  New  York  State  Cab.  Nat.  Hist., 

p.  60,  figure.  Cambrian. 

[ Olenus ] vermontana  Hall,  1859 ; Pal.  New  York,  vol.  3,  p.  527,  figure. 

[ Paradoxides']  vermonti  Emmons,  1860;  Manual  Geology,  p.  280  (note  A). 

[ Paradoxides ] vermontana  Barrande,  1861  ; Bull.  Soc.  G6ol.  France,  2d  series, 

vol.  18,  p.  277,  pi.  5,  fig.  8. 

[ Paradoxides  ] vermontana  Billings,  1861 ; Geology  Vermont,  vol.  2,  p.  950. 

\_Barrandia]  vermontana  Hall,  1861.;  13th  Rept.  New  York  State  Cab.  Nat. 

Hist.,  p.  117,  figure. 

[ Barrandia ] vermontana  Hall,  1861 ; Geol.  Vermont,  vol.  1,  p.  370,  pi.  13,  figs. 

2,  4,  and  5. 

[ Paradoxides ] vermontana  Billings,  1863 ; Geol.  Canada,  p.  953. 

[ Olenellus]  vermontana  Hall,  1862 ; 15th  Rept.  New  York  State  Cab.  Nat.  Hist., 

p.  114. 

[ OleneUus ] vermontana  Billings,  1865  ; Pal.  Foss.,  vol.  1,  p.  10. 

[ Olenellus ] vermontana  Whitfield,  1884;  Bull.  Am.  Mus.  Nat.  Hist.  New  York, 

vol.  1,  p.  152,  pi.  15,  figs.  2-4. 

vermontana  Walcott,  1885;  Am.  Jour.  Sci.,  3d  series,  vol.  29,  p.  329,  figs.  1,2. 

vermontana  Walcott,  1885;  Nature,  vol.  32,  p.  68. 

vermontana  Walcott,  1886;  Bull.  U.  S.  Geol.  Survey,  No.  30,  p.  158,  pi.  24, 

figs.  1 a,  b. 

Microdiscus  Emmons,  1855;  Am.  Geology,  vol.  1,  pt.  2,  p.  116. 

Type,  Microdiscus  speciosus  Ford. 

belli-marginatus  Shaler  and  Foerste,  1888;  Bull.  Mus.  Comp.  Zool.  Harvard 

Coll.,  vol.  16,  p.  35,  pi.  2,  fig.  19.  Cambrian. 

connexus  Walcott,  1887 ; Am.  Jour.  Sci.,  3d  series,  vol.  34,  p.  194,  pi.  1,  figs.  4-4  b. 

Cambrian. 

dawsoni  Hartt,  1868;  Acadian  Geology,  p.  654,  fig.  228.  St.  John. 

Mr.  Hartt  originally  described  this  species  under  the  new  generic  name  of 
Daivsonia,  but  on  Mr.  E.  Billings’s  authority  the  species  was  referred  to  Micro- 
discus in  the  Acadian  Geology. 

dawsoni  Whiteaves,  1878;  Am.  Jour.  Sci.,  3d  series,  vol.  16,  p.  225. 

dawsoni  Walcott,  1884;  Bull.-U.  S.  Geol.  Survey, No.  10,  p.  23,  pi.  2,  figs.  3,  3 a. 

[Agnostus]  lobatus  Hall,  1847 ; Pal.  New  York,  vol.  1,  p.  258,  pi.  67,  figs.  5 a-f. 

Potsdam. 

[Agnostus]  lobatus  Rogers,  1858;  Geol.  Survey  Pennsylvania,  vol.  2,  p.  820, 

fig.  614  (1-4). 

lobatus  Ford,  1873;  Am.  Jour.  Sci.,  3d  series,  vol.  6,  p.  135  (foot-note). 

lobatus  Walcott,  1886  j’Bull.  U.  S.  Geol.  Survey,  No.  30,  p.  156,  pi.  16,  figs.  1, 1 a,  b. 

lobatus  Shaler  and  Foerste,  1888;  Bull.  Mus.  Comp.  Zool.  Harvard  Coll.,  vol. 

16,  p.  36,  pi.  2,  fig.  13. 

meeki  Ford,  1876;  Am.  Jour.  Sci.,  3d  series,  vol.  11,  p.  371.  Lower  Potsdam. 

meeki  Walcott,  1886;  Bull.  U.  S.  Geol.  Survey,  No.  30,  p.  155,  pi.  16,  fig.  4. 

parkeri  Walcott,  1886  ; Bull.  U.  S.  Geol.  Survey,  No.  30,  p.  157,  pi.  16,  figs.  2, 2 a. 

Middle  Cambrian. 

pulchellus  (Hartt  MS.)  Walcott,  1884;  Bull.  U.  S.  Geol.  Survey,  No.  10,  p.  24. 

St.  John. 

punctatus  Salter,  1864  ; Quart.  Jour.  Geol.  Soc.  London,  vol.  20,  p.  237,  pi.  13, 

n-  St.  John! 

punctatus  Whiteaves,  1878;  Am.  Jour.  Sci.,  3d  series,  vol.  16,  p.  225. 


[BULL.  63. 


126  A BIBLIOGRAPHY  OF  PALEOZOIC  CRUSTACEA. 

Miciodiscus  punctatus  Walcott,  1884;  Bull.  U.  S.  Geol.  Survey,  No.  10,  p.  24,  pi.  2, 

figs.  1,  1 a-c. 

quadricostatus  Emmons,  1855 ; Am.  Geology,  vol.  1,  pt.  2,  p.  116,  pi.  1,  fig.  8. 

Taconic. 

quadricostatus  Emmons,  1860;  Manual  Geology,  p.  88,  fig.  73. 

quadricostatus  Barrande,  1861;  Bull.  Soc.  Gdol.  France,  2d  series,  vol.  18,  p. 

280,  pi.  5,  figs.  13  a,  b. 

speciosus  Ford,  1873 ; Am.  Jour.  Sci.,  3d  series,  vol.  6,  p.  137,  figs.  2 a,  b. 

Potsdam. 

speciosus  Ford,  1877  ; Am.  Jour.  Sci.,  3d  series,  vol.  13,  p.  147. 

speciosus  Ford,  1879 ; New  York  Tribune  Extra,  Sept.  2, 18/9,  fig.  2. 

speciosus  Walcott,  1886;  Bull.  U.  S.  Geol.  Survey,  No.  30,  p.  154,  pi.  16,  figs.  3, 

3 a— c. 

Nileus  Dalman,  1826  ; Palaead.,  p.  246  (German  trans.,  p.  49). 

Type,  Nileus  armadillo  Dalman. 

affinis  Billings,  1865;  Pal.  Foss.,  vol.  l,p.  275,  figs.  261  a,  b.  Quebec. 

macrops  Billings,  1865;  Pal.  Foss.,  vol.  1,  p.  273,  fig.  259.  Quebec. 

scrutator  Billings,  1865;  Pal.  Foss.,  vol.  1,  p.  274,  fig.  260.  Quebec. 

Nuttania  Eaton,  1832  (in  part) ; Geological  Text  Book,  p.  33.  (See  Trinucleus  and 
Homalojiotus. ) 

concentrica  Eaton,  1832;  Geological  Text  Book,  p.  34,  pi.  1,  fig.  2. 

sparsa  Eaton,  1832;  Geological  Text  Book,  p.  34. 

Odontoceplialus  Conrad,  1840 ; 3d  Ann.  Rept.  Pal.  Dept.  New  York  Geol.  Survey,  p.  204. 

IDalmanites  ( Odontoceplialus )]  Hall  and  Clarke,  1888;  Pal.  New  York,  vol.  7, 

p.  xxxiii.  m 

I can  not  do  justice  to  this  genus  without  giving  a brief  historical  sketch, 
which  dates  back  to  1781.  During  this  year  M.  T.  Briinnich  (Beskrivelse  over 
Trilobiten,  Nye  Samling  af  det  Kong.  Danske  Yidensk.  Skrifter,  vol.  1,  p.  392, 
pi.  0,  figs.  1 , 2)  published  a description  of  a fossil  Trilobite  from  Coalbrook  Dale 
under  the  name  of  Trilobus  caudatus.  As  this  Trilobite  in  after  years  had  many 
generic  names,  I give  a translation  of  the  original  description  for  the  use 
of  students.  The  author  figures  the  head  and  pygidium  of  Trilobus  caudatus 
and  remarks:  “As  I was  not  fortunate  enough  to  obtain  a complete  speci- 
men of  the  entirely  unknown  fossil,  but  only  broken  parts,  I can  not  distinctly 
describe  its  size  or  number  of  rings;  however,  the  annexed  figures  show 
the  distinct  features  of  this  species  and  their  peculiar  morphology.  The  size 
of  the  fossil  at  its  anterior  bend  is  If  inches,  the  front  piece  outside  of  the 
crust  is  £ inch,  its  total  length  34  inches;  the  broken  back  part,  consisting 
of  about  sixteen  rings,  is  1 inch  in  length  to  the  tail,  the  latter  being  1 inch 
long.  The  head  shield  is  surrounded  by  a flat-shaped  edge,  which  terminates 
in  an  upright  protuberance  with  a tongue  rounded  anteriorly.  The  shell 
shows  various  elevations  separated  by  transverse  furrows.  The  eyes  on  the 
side  of  the  shell  are  very  protruding,  semilunar  in  form,  and  faceted  after  the 
eyes  of  insects.  On  the  head-shield  may  be  seen  some  small  nodes,  which 
are  also  visible  on  the  first  ring  and  on  some  of  the  others.  The  tail  di- 
minishes in  breadth  and  terminates  in  a narrow,  long,  and  pointed  projec- 
tion. 

The  first  systematic  writer  (Brongniart,  Crust.  Foss.,  p.  22)  included  this 
species  under  his  genus  Asaphus,  and  it  was  so  classified  until  1844,  when  Dr.  H. 
F.  Emmrich  (Zur  Morphologic  der  Trilobiten,  p.  15,  pi.  1,  fig.  1)  proposed  the  new 
generic  term  of  Dalmania  for  it.  Unfortunately  this  term  was  then  preoccupied 
for  a genus  of  the  Diptera.  Dr.  H.  F.  Emmrich’s  work  was  well  known  in 
Europe,  having  appeared  in  two  separate  German  editions,  and  also  in  English 
(Scient.  Mem.,  vol.  4,  pt.  14,  1847). 

In  the  year  1847  A.  J.  C.  Corda  (Prodr.,  p.  208,  pi.  5,  fig.  56)  changed  Eimnrich’s 
generic  name  to  Odontochile,  a preoccupied  term  in  natural  history.  This  name 


V0GDE8.] 


CATALOGUE  OF  TRILOBITES. 


127 


was  only  used  by  one  other  author  (McCoy,  Annals  Nat.  Hist.,  London,  vol.  4, 
1849),  all  others  using  Dalmania  or  its  modified  form,  Dalmanites  (Barrande). 

In  1840  Milne-Ed wards  (Crust.,  pp.  306,339)  proposed  the  name  of  Pleura- 
canthus  for  Calymene  arachnoides  Goldfuss,  and  Dr.  Goldfuss  that  of  Acaste 
(Neues  Jahrbuch  fiir  Mineral.,  1843,  p.  511)  for  such  forms  as  Calymene  dozening  ice 
Murch. 

In  America  a typical  species  ( Dalmanites  limulurus ) has  been  classed  by  all 
American  writers  either  under  Dalmania  or  its  modified  form,  but  other  species 
properly  of  this  geuus — that  is,  if  we  do  not  desire  to  overburden  generic  classi- 
fication— have  been  given  new  generic  names.  The  first  was  an  obscure  fossil 
• described  by  Dr.  Jacob  Green  (Am.  Jour.  Sci.,  1st  series,  vol.  32,  p.  343)  as  Cry- 
pheeus  bootlii,  a generic  term  preoccupied  for  a genus  of  the  Coleoptera  at  the 
time  it  was  used  by  l)r.  Green.  The  second  species  consists  of  a poorly  figured 
tail,  described  and  figured  by  Prof.  Amos  Eaton  (Geological  Text  Book,  p.  31, 
pi.  1,  fig.  1)  as  Asaphus  selenurus,  and  by  Dr.  Jacob  Green  under  the  name  of 
Calymene  odontocephala  (Am.  Jour.  Sci.,  1st  series,  vol.  25,  p.  334).  Prof.  Amos 
Eaton’s  description  was  drawn  from  the  tail  of  the  fossil  and  Dr.  Jacob  Green’s 
from  the  head. 

Mr.  T.  A.  Conrad  in  1840  (3d  Ann.  Rept.  Pal.  Dept.  New  York  Geol.  Survey,  p. 
204)  procured  a perfect  specimen  of  this  Trilobite  and  united- the  two  species 
under  a new  generic  name.  Odontoceplialus  selenurus,  taking  Dr.  Jacob  Green’s 
specific  name  for  the  genus,  and  that  of  Prof.  Amos  Eaton  for  the  species. 

The  generic  characteristics  consist  of  a series  of  incisor-like  denticulations 
bordering  the  frontal  margin  of  the  head,  and  a pygidium  with  two  terminal 
spines. 

Hall  and  Clarke  (1888,  Pal.  New  York,  vol.  7,  p.  xxxiii)  use  the  term  as  a 
subgenus  to  Dalmanites. 

If  we  follow  the  strict  rule  of  priority  and  set  aside  the  preoccupied  name 
Dalmania  or  Dalmanites  for  that  of  Odontoceplialus  Conrad,  we  take  for  a generic 
name  a term  indicating  a denticulated  cephalic  shield,  which  is  confined  to  a 
special  group  and  miscall  such  species  as  the  well  known  type  Dalmanites 
caudatus. 

We  would  therefore  suggest,  not  only  in  honor  of  the  learned  Swedish  author 
on  Trilobites,  but  also  through  courtesy,  that  the  generic  name  of  Dalmanites 

be  retained. 

Odontoceplialus.  (See  Dalmanites  [ Odonfocepnalus  ] selenurus,  D.  [Odontoceplialus] 
bifidens,  D.  [Odontoceplialus']  aegeria,  and  D.  [Odontoceplialus]  coronatus. 

Ogygia  Brongniart,  1822;  Crust.  Foss.,  p.  26. 

Type,  Asaphus  buchii  Brongniart,  pi.  2,  figs.  3 a-c. 

[Asaphus]  barrandi  Hall,  1851;  Rept.  Geol.  Lake  Superior  Land  Dist.  (Foster 

and  Whitney),  pt.  2,  p.  210,  pi.  27,  figs.  1 a-d ; pi.  28.  Birdseye. 

[Asaphus]  barrandi  Hall,  1862;  Geol.  Wisconsin,  vol.  1,  p.  41,  fig.  4. 

klotzi  Rominger,  1887 ; Proc.  Acad.  Nat.  Sci.  Phila.,  p.  12,  pi.  1,  fig.  1. 

Cambrian. 

klotzi  Walcott,  1888;  Am.  Jour.  Sci.,  3d  series,  vol.  36,  p.  166. 

[OgyyieH]  latissimus  Eaton,  1832;  Am.  Jour.  Sci.,  vol.  21,  p.  136,  foot-note. 

[Ogyges]  latissimus  Eaton,  1832;  Geol.  Text  Book,  p.  33  (Homalonotus  delphi- 

nocephus). 

parabola  Hall  and  Whitfield,  1877 ; U.  S.  Geol.  Expl.  40th  Par.,  vol.  4,  p.  245,  pi. 

2,  fig.  35.  Cambrian. 

? problematica  Walcott,  1.884;  Pal.  Eureka  Dist.,  Mon.  U.  S.  Geol.  Survey,  vol. 

8,  p.  63,  pi.  10,  figs.  2 a,  b and  4.  Cambrian. 

producta  Hall  and  Whitfield,  1877  ; U.  S.  Geol.  Expl.  40th  Par.,  vol.  4,  p.  234, 

pi.  2,  figs.  31-34 ; also  p.  245,  pi.  2,  fig.  35.  Cambrian. 

[Nio&e]  producta  Brogger,  1886;  Om  alderen  af  Olonellus  zonm  i Nordamerika, 

p.  211. 


128  A BIBLIOGRAPHY  OF  PALEOZOIC  CRUSTACEA.  [bull.  63. 

Ogygia  [ Bathyuriscus ] productus  Walcott,  1886;  Bull.  U.  S.  Geol.  Survey,  No.  30,  p. 
217,  pi.  30,  figs.  1, 1 a-i. 

Syn.,  Ogygia  parabola  (H.  & W.)  Walcott,  1886;  idem.,  p.  217. 

serrata  Romiuger,  1887 ; Proc.  Acad.  Nat.  Sci.  Pliila.,  p.  13,  pi.  1,  figs.  2, 2a. 

Cambrian. 

? spinosa  Walcott,  1884;  Pal.  Eureka  Dist.,  Mon.  U.  S.  Geol.  Survey,  vol.  >8,  p. 

63,  pi.  9,  fig.  22.  (See  Olenoides  spinosa  Walcott.) 

vetustus  Hall,  1847 ; Pal.  New  York,  vol.  1,  p.  227,  pi.  60,  fig.  1.  Trenton. 

vetustus  Emmons,  1855;  American  Geology,  vol.  1,  pt.  2,  p.  216,  fig.  72. 

Olenellus  Hall,  1861;  Des.  N.  Species  of  Foss.,  published  in  advance,  15tli  Rept. 
State  Cab.,  p.  86.  Hall,  1862 ; 15th  Rept.  State  Cab.  Nat.  Hist.  Albany,  p.  114. 
Type,  Olenellus  thompsoni  Hall. 

[ Elliptocephala ] asaphoides  Emmons,  1844  ; Taconic  System,  p.  21,  figs.  1-3. 

Cambrian. 

[ Elliptocephala ] asaphoides  Emmons,  1846;  Agric.  New  York,  vol.  1,  p.  65,  figs. 

1-3. 

[ Olenus]  asaphoides  Hall,  1847  ; Pal.  New  York,  vol.  1,  p.  256,  pi.  67,  figs.  2 a,  c. 

[Olenus]  asaphoides  Fitch,  1849;  Trans.  N.  Y.  State  Agric.  Soc.,  vol.  9. p.865. 

[ Elliptocephalus ] asaphoides  Emmons,  1849;  Proc.  Am.  Assoc.  Adv.  Sci.,  1st 

meeting,  p.  18. 

— — [Eliptocephalns]  asaphoides  Emmons,  1855 ; Am.  Geology,  vol.  1.  pt.  2,  p.  114, 
figs.  1-3,  pi.  1,  fig.  18. 

[ Paradoxides ] asaphoides  Emmons,  1860;  Manual  Geology,  pp.  87,280. 

[Paradoxides]  asaphoides  Barrande,  1861;  Bull.  Soc.  G6ol.  France,  2d  series, 

vol.  18,  p.  273,  pi.  5,  figs.  4, 5. 

[Olenus]  asaphoides  Ford,  1871 ; Am.  Jour.  Sci.,  3d  series,  vol.  2,  p.  33. 

[Elliptocephalus]  asaphoides  Ford,  1877 ; Am.  Jour.  Sci.,  3d  series,  vol.  13,  p. 

266,  plate,  figs.  1-10. 

[ Elliptocephalus ] asaphoides  Ford  ; Am.  Jour.  Sci.,  3d  series,  vol.  15,  p.  129. 

asaphoides  Ford,  1881 ; Am.  Jour.  Sci.,  3d  series,  vol.  22,  p.  250. 

asaphoides  Walcott,  1886;  Bull.  U.  S.  Geol.  Survey,  No.  30,  p.  168,  pi.  17,  figs.  4, 

8, 10  ; pi.  20,  figs.  3, 3 a,  b ; pi.  25,  fig.  8. 

gilberti  (Meek  MS.)  White,  1874;  Prelim.  Rept.  Invt.  Foss.  U.  S.  Geog.  and 

Geol.  Survey  West  100th  Mer.,  p.  7.  Potsdam. 

[ Olenus]  gilberti  Gilbert,  1875  ; U.  S.  Geog.  Survey  West  100th  Mer.,  vol.  3,^.  182. 

gilberti  White,  1877 ; U.  S.  Geog.  Survey  West  100th  Mer.,  vol.  4,  p.  44,  pi.  2,  figs. 

1, 3 a-e. 

gilberti  Walcott,  1884 ; Pal.  Eureka  Dist.,  Mon.  U.  S.  Geol.  Survey,  vol.  8,  p.  29, 

pi  9,  figs.  16, 16  a ; pi.  21,  fig.  13. 

gilberti  Walcott,  1886;  Bull.  U.  S.  Geol.  Survey,  No.  30,  p.  170,  pi.  18,  figs.  1,  1 

a-c ; pi.  19,  fig.  2,  2 a-k ; pi.  20,  figs.  1,  1 a,  1 b,  4. 

howelli  (Meek  MS.)  White,  1874;  Prelim.  Rept.  Invt.  Foss.  U.  S.  Geog.  and 

Geol.  Survey  West  100th  Mer.,  p.  8.  Potsdam. 

[Olefins']  howelli  Gilbert,  1875;  U.  S.  Geog.  Survey  West  100th  Mer.,  vol.  3,  p. 

183. 

howelli  White,  1877;  U.  S.  Geog.  Survey  West  100th  Mer.,  vol.  4,  p.  47,  pi.  2f  i 

• figs.  4 a,  b. 

— » — howelli  Walcott,  1884;  Pal.  Eureka  Dist.,  Mon.  U.  S.  Geol.  Survey,  vol.  8,  pp.  « 
29,  30,  pi.  9,  figs.  15a-b,  16-16 a;  pi.  21,  figs.  1-9. 

iddingsi  Walcott,  1884  ; Pal.  Eureka  Dist.,  Mon.  U.  S.  Geol.  Survey,  vol.  8,  p.  • 

28,  pi.  9,  fig.  12.  Cambrian.  ^ 

iddingsi  Walcott,  1886;  Bull.  U.  S.  Geol.  Survey,  No.  30,  p.  170,  pi.  19,  fig.  1. 

[Paradoxides]  macrocephalus  Emmons,  1860;  Manual  Geology,  p.  88,  fig.  70. 

[Olenus]  thompsoni  Hall,  1859;  12th  Rept.  New  York  State  Cab.  Nat.  Hist.,  p. 

57,  figure.  Cambrian,  ) 


VOGDES.l 


CATALOGUE  OF  TRILOBITES. 


129 


Olenellus  [ Olenus ] thompsoni  Hall,  1859  ; Pal.  New  York,  vol.  3,  p.  525,  figure. 

I Barr  an  dial  thompsoni  Hall,  1860  ; 13th  Rept.  New  York  State  Cab.  Nat.  Hist., 

p.  116,  figure. 

[ Paradoxides ] thompsoni  Emmons,  1860  ; Mauual  Geology,  p.  280,  note  A. 

[ Paradoxides]  thompsoni  Barrande,  1861 ; Bull.  Soc.  G6ol.  France,  2d  series, 

vol.  18,  p.  276,  pi.  5,  fig.  6. 

[ Paradoxides ] thompsoni  Billings,  1861 ; Geol.  Vermont,  vol.  2,  p.  950. 

[Barrandia]  thompsoni  Hall,  1861 ; Geol.  Vermont,  vol.  2,  p.  369,  pi.  13,  fig.  1. 

[ Paradoxides ] thompsoni  Billings,  1861 ; Pal.  Foss.,  vol.  1,  p.  11  (pamphlet  pub- 
lished in  advance). 

thompsoni  Hall,  1862;  15th  Rept.  New  York  State  Cab.  Nat.  Hist,  p.  114. 

thompsoni  Billings,  1863;  Geol.  Canada,  p.  953. 

[ Olenellus ] thompsoni  Billings,  1865;  Pal.  Foss.,  vol.  1,  p.  11. 

thompsoni  Whitfield,  1884;  Bull.  Am.  Mus.  Nat.  Hist.,  New  York,  vol.  l,p.  151 

pi.  15,  figs.  1-4. 

thompsoni  Walcott,  1886;  Bull.  U.  S.  Geol.  Survey,  No.  30,  p.  167,  pi.  17,  figs. 

1, 2,  4, 9 ; pis.  22, 23,  figure. 

vermontana.  (See  Mesonacis  vermontana  (Hall)  Walcott.) 

Olenoides  Meek,  1877 ; U.  S.  Geol.  Expl.  40th  Par.,  Pal.,  vol.  4,  p.  25. 

Type,  Olenoides  nevadensis  Meek. 

fordi  Walcott,  1887  ; Am.  Jour.  Sci.,  3d  series,  vol.  34,  p.  195,  pi.  1,  figs.  5,  5 b. 

Cambrian. 

flagricaudus.  (See  Zacanthoides  flagricaudus.) 

levis  Walcott,  1886  ; Bull.  U.  S.  Geol.  Survey,  No.  30,  p.  187,  pi.  25,  figs.  3-3  a. 

(See  Zacanthoides  levis.)  Cambrian. 

gothicus  (Hall  and  Whitfield)  Walcott.  (See  Dorypyge  gothicus.) 

? marcoui  Walcott,  1886;  Bull.  U.  S.  Geol.  Survey,  No.  30,  p.  186,  pi.  26,  fig. 

5-5  a,  b. 

[ Dikellocephalus  ?]  marcoui  Whitfield,  1884 ; Bull.  Am.  Mus.  Nat.  Hist.  New 

York,  vol.  1,  p.  150,  pi.  14,  fig.  7.  Cambrian. 

[Paradoxides  f ] nevadensis  Meek,  1870 ; Proc.  Acad.  Nat.  Sci.  Phila.,  vol.  22,  p.  62. 

Middle  Cambrian. 

[Paradoxides?]  nevadensis  Meek,  1877 ; U.  S.  Geol.  Expl.  40th  Par.,  Pal.,  vol. 

4,  p.  23,  pi.  1,  fig.  5. 

ifevadensis  Meek,  1877 ; U.  S.  Geol.  Expl.  40th  Par.,  Pal.,  vol.  4,  p.  25. 

nevadensis  Walcott,  1886;  Bull.  U.  S.  Geol.  Survey,  No.  30,  p.  181,  pi.  25,  fig.  7. 

nevadensis  Walcott,  1888 ; Am.  Jour.  Sci.,  3d  series,  vol.  36,  p.  165. 

Syn.,  Ogygia  serrata  (Rominger)  Walcott,  1888;  Am.  Jour.  Sci.,  3d  series,  vol.  36, 

p.  165. 

[Olenoides]  quadriceps  (Hall  and  Whitfield)  Walcott.  (See  Dorypyge  quadri- 
ceps.) 

spinosus.  (See  Zacanthoides  spinosus.) 

tgpicali8.  (See  Zacanthoides  typicalis.) 

[ Dikellocephalm ] wahsatchensis  Hall  and  Whitfield,  1877 ; U.  S.  Geol.  Expl. 

40th  Par.,  Pal.,  vol.  4,  p.  241,  pi.  1,  fig.  35. 

wahsatchensis  Walcott,  1886 ; Bull.  U.  S.  Geol.  Survey,  No.  30,  p.  189,  pi.  29, 

figs.  2,2  a.  Middle  Cambrian. 

Syn.,  [Dikellocephalus?]  gothicus  (Hall  and  Whitfield)  Walcott,  1886;  Bull.  U.  S. 
Geol.  Survey,  No.  30,  p.  189. 

wahsatchensis  Walcott,  1888;  Am.  Jour.  Sci.,  3d  series,  vol.  36,  p.  165. 

Olenus  Dalman,  1826 ; Pahead,  p.  226. 

Type,  Olenus  gibbosus  Wahlcnberg. 

asaphoides.  (See  Olenellus  asaphoides.) 

— ■ — holopyga.  (See  Bathynotus  holopyga.) 

logani.  (See  Ptychoparia  logani.) 

Bull.  03 9 


130 


A BIBLIOGRAPHY  OF  PALEOZOIC  CRUSTACEA. 


[BULL.  63. 


Olenus  thompsoni.  (See  Olenellus  thompsoni.) 

undulostriatus  Hall,  1847 ; Pal.  New  York,  vol.  1,  p.  258,  pi.  67,  figs.  3 a,b. 

Hudson. 

utahensis  Woodward,  1873 ; Rept.  43d  Meeting  Brit.  Assoc.  Adv.  Sci. 

utahensis  Woodward,  1873;  Geol.  Mag.,  vol.  10,  p.  523.  Cambrian. 

vermontana.  (See  IVlesonacis  vermontana  Hall.) 

Oryctcocephalus  Walcott,  1886 ; Bull.  U.  S.  Geol.  Survey,  No.  30,  p.  210. 

primus  Walcott,  188&  ; Bull.  U.  S.  Geol.  Survey,  No.  30,  p.  210,  pi.  29,  figs.  3,  3 a. 

Middle  Cambrian. 

Pagura  Emmons,  1860  ; Manual  Geology,  p.  280. 

Dr.  E.  Emmons  uses  this  term  in  a subgeneric  sense  for  Paradoxides  [ Pagura ] 
quadrispinosus.  The  note  accompanying  the  Manual  of  Geology  does  not  indi- 
cate the  author’s  intentions  with  regard  to  the  genus  and  new  species.  It  was 
probably  intended  for  Paradoxides  [ Peltura ] quadrispinosus,  a synonym  of  in- 
tended Peltara  yOlenus']  holopyga  Hall,  12th  Rept.  New  York  State  Cab.  Nat. 
Hist.,  p.  61.  Emmons  figures  this  species  on  p.  80,  fig.  57. 

Fanderia  Yolborth  ; Mem.  Acad.  Sci.  St.-Pdtersbourg,  vol.  6,  p.  31. 

Type,  Panderia  triquetra  Volb.,  pi.  3,  fig.  13  bis,  17. 

_ \IUoenu8-\  conradi  Billings,  1859 ; Canadian  Naturalist,  vol.  4,  p.  372,  figs.  7-9. 

L Trenton. 


For  other  references,  see  Illcenus  conradi  Billings. 

Paradoxides  Brongniart,  1822;  Crust.  Foss.,  p.  30,  pi.  4,  fig.  1. 

Type,  Paradoxides  tessini  Brongniart. 

Syn.,  Plutonia  Salter,  1869;  Quart.  Jour.  Geol.  Soc.  London,  vol.  25,  p.  52. 

Plutonia  sedgwicki,  Quart.  Jour.  Geol.  Soc.  London,  vol.  27,  p.  399,  pi.  15, 
1~8. 

acadicus  Matthew,  1882;  Trans.  Roy.  Soc.  Canada,  vol.  1,  p.  103,  pi.  9,  figs. 

16  18  Jol-in. 

acadicus  Matthew,  1884;  Trans.  Roy.  Soc.  Canada,  vol.  2,  p.  99,  pi.  1,  fig.  1. 

acadicus  Walcott,  1884;  Bull.  U.  S.  Geol.  Survey,  No.  10,  p.  25,  pi.  6,  figs.  3-3  a. 

arcuatus  Harlan.  (See  Triarthrus  beckii.) 

barberi  Winchell,  1884;  13th  Rept.  Geol.  Nat.  Hist.  Survey  Minn,  p.  65,  pi.  1, 

„ _ Cambrian, 

kg-  7-  , ..  . 

beckii.  (See  Triarthrus  beckii.)  _ « 

bennetii  Salter,  1859;  Quart.  Jour.  Geol.  Soc.  London,  vol.  15,  p.  553,  figure. 

Cambrian. 

_ bennetii  Salter  and  Woodward,  1865;  Chart  of  Foss.  Crust.,  fig.  25. 

})oltoni.  (See  Lidias  boltoni.)  , 

decorus  Billings,  1865;  Pal.  Foss.,  vol.  2,  p.  75.  0 s ara* 

eatoni.  (See  Triarthrus  beckii.) 

eteminicus  Matthew,  1882 ; Trans.  Roy.  Soc.  Canada,  vol.  1,  p.  92,  pi.  9, 

Yar.  suricoides  (figs.  4-6),  var.  breviatus , var.  malicitus  (fig.  13),  var.  pontifi- 
cate (figs.  15,  15  a),  var.  quacoensis  (figs.  14,  14  a).  _ _ _ „ t 

eteminicus  Walcott,  1884;  Bull.  U.  S.  Geol.  Survey,  No.  10,  p.  27,  pi.  3,  figs.  1- 

harlani  Green,  1834;  Am.  Jour.  Sci.,  1st  series,  vol.  35,  p.  336.  Cambrian. 

harlani  Green,  1835 ; Suppl.  Mon.  Tril.  N.  A.,  p.  14,  cast  39. 

harlani  Rogers,  1856;  Proc.  Boston  Soc.  Nat.  Hist.,  vol.  6,  pp.  27,40. 

harlani  Stodder,  1856 ; Proc.  Boston  Soc.  Nat.  Hist.,  vol.  6,  p.  369. 

harlani  Rogers,  1856;  Am.  Jour.  Sci.,  2d  series,  vol  22,  p.  297 

Svn.,  spinosus  Rogers,  1858;  Geol.  Pennsylvania,  vol.  2,  p.  816,  fig.  o90. 

harlani  Ordway,  1861 ; Proc.  Boston  Soc.  Nat.  Hist.,  vol.  8,  p.  1,  figure. 

harlani  Walcott,  1884;  Bull.  U.  S.  Geol.  Survey,  No.  10,  p.  45,  pi.  7,  fig.  3,  pi. 

8,  figs.  1>  1 a-c;  pi.  9,  fig.  1? 


VUGDKS.J 


CATALOGUE  OF  TRILOBITES. 


131 


Paradoxides  kjerulfi  (Linrs.)  Matthew,  1886 ; Am.  Jour.  Sci.,  3d  series,  vol.  31,  p. 
471.  Cambrian. 

Referred  by  Holm  (Geol.  Foren.  Stockholm  Forhandl.,  vol.  9,  1887,  hafte.  7, 
p.  1)  to  Olenellus  kjerulfi  Linnarsson,  pis.  14  and  15. 

lamellatus  Hartt,  1868;  Acadian  Geology,  p.  656,  fig.  230.  .St.  John. 

lamellatus  Matthew,  1882  ; Trans.  Royal  Soc.  Canada,  vol.  1,  p.  100,  pi.  1,  figs. 

3,4.  1 

lamellatus  var.  loricatus  Matthew,  1882;  Trans.  Royal  Soc.  Canada,  vol.  1,  p. 

105,  pi.  9,  fig.  19. 

lamellatus  Walcott,  1884;  Bull.  U.  S.  Geol.  Survey,  No.  30,  p.  25,  pi.  3,  figs. 

2, 2 a. 

macrocephalus.  (See  Olenellus  thompsoni  Hall.) 

micmac  Hartt,  1868;  Acadian  Geology,  p.  657.  St.  John. 

micmac  Matthew,  1884 ; Trans.  Royal  Soc.  Canada,  vol.  2,  p.  101,  pi.  10,  fig.  8. 

? nevadcnsis.  (See  Olenoides  nevadensis.) 

quadrispinosus.  (See  Bathynotus  quadrispinosus.) 

tenellus  Billings,  1874;  Pal.  Foss.,  vol.  2,  p.  74,  fig.  43.  Potsdam. 

thompsoni.  (See  Olenellus  thompsoni  Hall.) 

triarihrus  Harlan ; Trans.  Geol.  Soc.  Pennsylvania,  vol.  1,  p.  264,  pi.  15,  fig.  5. 

(See  Triarthrus  becki  Green.) 

vermontana.  (See  Olenellus  and  Mesonacis.) 

walcotti  Shaler  and  Foerste,  1888;  Bull.  Mus.  Comp.  Zool.  Harvard  Coll.,  vol. 

16,  p.  36,  pi.  2,  fig.  12.  . Cambrian. 

Peltura  Milne-Edwards,  1840;  Crust.,  vol.  3,  p.  344. 

(See  Pagura.) 

liolopyge.  (See  Bathynotus  holopyge.) 

Pemphigaspis  Hall,  1863;  16th  Rept.  New  York  State  Mus.  Nat.  Hist.,  p.  221. 

bullata  Hall,  1863 ; 16th  Rept.  New  York  State  Mus.  Nat.  Hist.,  p.  221,  pi.  5 a, 

figs.  3-5.*  Potsdam. 

A species  probably  of  the  genus  Microdiscus. 

Phacops  Emmrich,  1839;  De  Trilobites,  etc.,  p.  18. 

Type,  Calymene  latifrons  Broun. 

The  generic  term  Trimerocephalus  McCoy  has  been  used  by  authors  for  species 
like  Phacops  volborthi, compact  in  form ; glabella  inflated  and  expanded  in  front; 
lobes,  except  the  basal  ones,  obscure;  eyes  small  and  occupying  the  front  por- 
tions of  the  head ; genal  angles  rounded ; pleura  rounded ; pygidium  small,  with 
few  segments,  and  even  border. 

Acaste  Goldfuss  for  such  species  as  Phacops  downingice  Mufch.  Diagnosis: 
Glabella  not  inflated  nor  greatly  expanded  in  front ; furrows  distinct ; eyes 
well  developed,  with  numerous  lenses;  genal  angles  produced  into  spines; 
pleurm  rounded  or  truncate ; pygidium  small  generally,  with  less  than  eleven 
segments  ; border  even,  but  sometimes  mucronate. 

[ Calymene ] bufo  Green,  1832;  Monthly  Am.  Jour.  Geol.,  p.  559. 

ICalymeue ] bufo  Green,  1832;  Mon.  Tril.  N.  A.,  p.  41,  cast  10. 

bufo  Hall,  1861 ; Des.  New  Species  Foss.,  p.  65. 

bufo  Hall,  1862;  15th  Rept.  New  York  State  Cab.  Nat.  Hist.,  p.  93. 

bufo  Hall,  1876;  Ulus.  Devonian  Foss.  Crust.,  pi.  8,  figs.  24,25. 

bufo  Hall,  1888;  Pal.  New  York,  vol.  7,  p.  26, 'pi.  8,  figs.  25/26. 

The  fossil  is  said  to  have  been  found  in  a dark  grayish  limestone  in  the  State 
of  New  Jersey.  The  cast  approaches  so  near  Phacops  latifrons  Broun  that  it 
may  be  the  same  species. 

bombifrons.  (See  Phacops  cristata.) 

cacapona  Hall,  1861 ; Des.  New  Species  Foss.,  p.  68.  Hamilton. 

Syn.,  Calymene  bufo  Castelnau,  1843;  Syst.  Sil.  do  I’Ainer.,  p.  21,  pi.  2,  figs.  1-4. 
cacapona  Hall,  1862;  15th  Rept.  New  York  State  Cab.  Nat.  Hist.,  p.  96. 


132 


A BIBLIOGRAPHY  OF  PALEOZOIC  CRUSTACEA. 


[BULL.  63. 


Phacops  cacapona  Hall,  1876  ; Illus.  Devonian  Foss.  Crust.,  pi.  8,'  figs.  18-23. 

cacapona  Hall,  1888;  Pal.  New  York,  vol.  7,  p.  27,  pi,  8,  figs.  19-24. 

callicephala.  (See  Dalmanites  callicephala. ) 

cristata  Hall,  1861 ; Des.  New  Species  Foss.,  p.  67.  Upper  Helderberg. 

Syn.,  Phacops  homhifrons  Hall,  1861 ; Des.  New  Species  Foss.,  p.  67. 

Phacops  cristata  Hall,  1862;  15th  Rept.  New  York  State  Cab.  Nat.  Hist.,  p.  95. 
Phacops  cristata  Hall,  1876  ; Illus.  Devonian  Foss.  Crust.,  pi.  6,  figs.  1-17. 
Phacops  homhifrons  Hall,  1876;  Illus.  Devonian  Foss.  Crust.,  pi.  6,  figs.  18-29. 
- — cristata  Hall,  1888;  Pal.  New  York,  vol.  7,  p.  14,  pi.  6,  figs.,  1-31,  16-29;  pi. 
8 a,  figs.  1-4. 

cristata  var.  pipa  Hall,  1888;  Pal.  New  York,  vol.  7,  p.  18,  pi.  8 a,  figs.  .5-18. 

Upper  Helderberg. 

doivningce  Murcb.  (See  Phacops  trisulcatus  Hall.) 

— — hudsonica  Hall,  1859;  Pal.  New  York,  vol.  3,  p.  355,  pi.  73,  figs.  26-28. 

Lower  Helderberg. 

f laticauda  Hall,  1847  ; Pal.  New  York,  vol.  1,  p.  248,  pi.  64,  fig.  6.  (See  Dalmani- 
tes micrurus  Green.) 

logani  Hall,  1859 ; Pal.  New  York,  vol.  3,  p.  353,  pi.  73,  figs.  15-25. 

Lower  Helderberg. 

[ Cahjmene~\  macrophthalma  Green,  1832;  Mon.  Tril.  N.  A.,  p.  39,  cast  9. 

[ Calymene']  nupera  Hall,  1843;  Geol.  New  York,  4th  Geol.  Dist.,  p.  262,  fig.  116. 

Chemung. 

nupera  Emmons,  1869  ; Manual  Geology,  p.  149,  fig.  138  (2). 

nupera  Hall,  1876;  Illus.  Devonian  Foss.  Crust.,  pi.  8,  fig.  26. 

nupera  Hall,  T888;  Pal.  New  York,  vol.  7,  p.  27,  pi.  8,  fig.  27. 

orestes  Billings,  1860  ; Canadian  Naturalist,  vol.  5,  p.  65,  fig.  10. 

Middle  Silurian. 

pulchellus  Foerste,  1887  ; Bull.  Denison  Univ.,  vol.  2,  p.  99,  pi.  8,  figs.  4,20,21. 

Clinton. 

\_Calymene  hufo]  var.  rana  Green,  1832;  Monthly  Am.  Jour.  Geol.,  p.  559. 

Hamilton. 

[ Calymene  hufo]  var.  rana  Green,  1832;  Mon.  Tril.  N.  A.,  p.  42,  casts  11, 12. 

ICalymene  hufo]  var.  rana  Hall,  1843;  Geol.  New  York,  4th  Geol.  Dist.,  p.  201, 

pi.  14. 

Syn.,  [ Calymene ] hufo  Owens,  1844  ; Geol.  Expl.  Iowa,  Wisconsin,  and  Illinois,  p. 
74,  pi.  12,  fig.  1. 

{Calymene]  hufo  Emmons,  1860  ; Manual  Geology,  p.  138,  wood-cutl24,  fig.  6. 
rana  Hal>,  1861 ; Description  New  Species  Fossils,  p.  65. 

rana  Hall,  1862 ; 15th  Rept.  New  York  State  Cab.  Nat.  Hist.,  p.  93,  pi.  10,  fig.  12. 

rana  Meek  and  Worthen,  1868 ; Geol.  Survey  Illinois,  vol.  3,  p.  447,  pi.  11,  figs. 

1 a-e. 

rana  Nicholson,  1873  ; Pal.  Province  Ontario,  p.  123,  figs.  5,6  a. 

rana  Hall,  1876;  Illus.  Devonian  Foss.  Crust.,  pi.  6,  figs.  14, 15;  pi.  7,  figs.  1-11  ; 

pi.  8,  figs.  11-17. 

rana  Whitfield,  1882;  Geol.  Wisconsin,  vol.  4,  p.  339,  pi.  26,  figs.  17-19. 

rana  Walcott,  1884  ; Pal.  Eureka  Dist.  Mon.  U.  S.  Geol.  Survey,  vol.  8,  p.  207. 

rana  Hall,  1888 ; Pal.  New  York,  vol.  7,  p.  19,  pi.  7,  figs.  1-11 ; pi.  8,  figs.  1-18 ; 

pi.  7 a,  figs.  21-33. 

rana  Clarke,  1888 ; Jour.  Morphology,  vol.  2,  p.  253,  pi.  21. 

traganus  Billings,  1863 ; Proc.  Portland  Soc.  Nat.  Hist.,  vol.  1,  p.  124,  pi.  1,  figs. 

26, 27.  Upper  Silurian. 

? trisulcatus  Hall,  1843 ; Geol.  New  York,  4th  Geol.  Dist.,  p.  72,  fig.  9. 

Clinton. 

trisulcatus  Hall,  1852 ; Pal.  New  York,  vol.  2,  p.  300,  pi.  66  a,  figs.  3 a,  b. 


VOGDES  1 


CATALOGUE  OF  TRILOBITES. 


133 


Phaethonides  Angelin,  1852  ; Pal.  Scand.,  p.  21. 

arenicolus  Hall,  1888 ; Pal.  New  York,  vol.  7,  p.  134,  pi.  25,  figs.  12, 13. 

Upper  Helderberg. 

denticulatus  (Meek)  Hall,  1888 ; Pal.  New  York,  vol.  7,  p.  139,  pi.  25,  tigs.  14, 15. 

For  other  references,  see  Proetus  [ Phceton~\  denticulatus  Meek. 

Steptoe  Valley,  Nevada,  Devonian  (?). 

gemmaeus  Hall,  1888;  Pal.  New  York,  vol.  7,  p.  136,  pi.  24,  figs.  32-36. 

Upper  Helderberg. 

immaturus  Herrick,  1889;  Bull.  Denison  Univ.,  vol.  4,  p.  59,  pi.  1,  tigs.  9-15. 

Kinderhook. 

(?)  lodiensis  (Meek)  Herrick,  1889;  Bull.  Denison  Univ.,  vol.  4,  p.  59. 

For  other  references,  see  Brachymetopus  lodiensis  Meek. 

occidentals  Herrick,  1889;  Bull.  Denison  Univ.,  vol.  4,  p.  57,  pi.  1,  figs.  10  a,  b. 

Kinderhook. 

sedaliensis  (Vogdes)  Herrick,  1839;  Bull.  Denison  Univ.,  vol.  4,  p.  57. 

Waverly. 

For  other  references,  see  Griffithides  ? sedaliensis  Vogdes. 

spinosus  Herrick,  1889;  Bull.  Denison  Univ.,  vol.  4,  p.  58,  pi.  1,  figs.  4-5. 

Kinderhook. 

varicella  Hall,  1888 ; Pal.  New  York,  vol.  7,  p.  135,  pi.  24,  figs.  29-31. 

Upper  Helderberg. 

Phillipsia  Portlock,  1843;  Kept.  Geol.  Londonderry,  etc.,  p.  315. 

Type,  Phillipsia  gemmulifera  Phillips. 

Dr.  Henry  Woodward  suggests  (Geol.  Mag.,  vol.  10,  1883)  the  following  brief 
diagnosis  of  the  characters  of  the  genera  Phillipsia  and  Griffithides,  which  may 
be  found  useful  in  separating  the  genera  : 


Phillipsia. 

Griffithides. 

1 

Sides  of  the  glabella  nearly  parallel 

Glabella  pyriform. 

2 

Marked  by  either  two  or  three  short  lat- 
eral furrows. 

No  short  lateral  furrows  on  the  glabella. 

3 

Basal  lobes  continuous  with  the  glabella.. 

Basal  lobes  distinct  from  the  glabella. 

4 

Eyes  large,  reniform 

Eyes  small,  suboval. 

bufo.  (See  Griffithides  bufo.) 

cliftonensis  Shumard,  1858  ; Trans.  Acad.  Nat.  Sci.  St.  Louis,  vol.  1,  p.  227. 

Coal  Measures. 

cliftonensis  Herrick,  1887 ; Bull.  Denison  Univ.,  vol.  2,  p.  11. 

cliftonensis  Vogdes,  1887 ; Annals  New  York  Acad.  Sci.,  vol.  4,p.  84. 

? consors  Herrick,  1889  ; Bull.  Denison  Univ.,  vol.  4,  p.  53,  pi.  1,  figs.  16  a,  b,  c. 

Keokuk  or  Burlington. 

consors  Herrick,  1890 ; American  Geologist,  vol.  5,  p.  254. 

f coronata.  (See  Cyphaspis  coronata  Hall.) 

dori8  (Hall)  Winchell,  1865;  Proc.  Acad.  Nat.  Sci.  Phila.,  2d  series,  vol.  9,  p. 

133.  (See  Proteus  doris  Hall.) 

howi  Billings,  1863  ; Canadian  Naturalist,  vol.  8,  p.  209,  figure.  Carboniferous. 

howi  Dawson,  1868;  Acadian  Geology,  p.  313,  fig.  133. 

howi  Herrick,  1887 ; Bull.  Denison  Uuiv.,  vol.  2,  p.  63. 

howi  Vogdes,  1887 ; Annals  New  York  Acad.  Sci.,  vol.  4,  p.  91. 

Compare  Phillipsia  meramecensis. 

insignis  Winchell,  1863;  Proc.  Acad.  Nat.  Sci.  Phila.,  2d  series,  vol.  7,  p.  24. 

Burlington. 

insignis  Billings,  1863;  Canadian  Naturalist,  vol.  8,  p.  209. 

insignia  Herrick,  1887;  Bull.  Denison  Univ.,  vol.  2,  p.  63. 


134 


A BIBLIOGRAPHY  OF  PALEOZOIC  CRUSTACEA. 


[BULL.  63. 


Phillipsia  insignis  Vogdes,  1887 ; Annals  New  York  Acad.  Sci.,  vol.  4,  p.  87. 

Icevis.  (See  Cyphaspis  laevis.) 

major  Shumard,  1858;  Trans.  Acad.  Sci.  St.  Louis,  vol.  1,  p.  226.  Coal  Measures. 

major  Meek,  1872;  U.  S.  Geol.  Survey  Territories,  Final  Rept.  Nebraska,  p.  238, 

pi.  3,  figs.  2 a,  b,  c. 

major  Herrick,  1887 ; Bull.  Denison  Univ.,  vol.  2,  p.  60. 

major  Vogdes,  1887 ; Annals  New  York  Acad.  Sci.,  vol.  4,  p.  85,  pi.  3,  fig.  14. 

meramecansis  Sbumard,  1855;  1st  and  2d  Rept.  Geol.  Survey  Missouri,  p.  199, 

pi.  B,  fig.  9.  Archimides  Limestone. 

meramecansis  Herrick,  1887 ; Bull.  Denison  Univ.,  vol.  2,p.  59. 

meramecansis  Vogdes,  1887 ; Annals  New  York  Acad.  Sci.,  vol.  4,  p.  86,  pi.  3, 

fig.  15. 

Syn.,  meramecansis ? Winchell,  1863 ; Proc.  Acad.  Nat.  Sci.  Phila.,  2d  series,  vol.  7, 
p.  24.  Keokuk. 

meramecansis  Herrick,  1888;  Bull.  Denison  Univ.,  vol.  3,  p.  28,  pi.  11,  fig.  3. 

Syn.,  howi  (Billings)  Vogdes,  1887 ; Annals  New  York  Acad.  Sci.,  vol.  4,  p.  92. 

vindobonensis  (Hartt)  Vogdes,  1887 ; Annals  New  York  Acad.  Sci.,  vol.  4, 
p.  92. 

meramecansis  Herrick,  1889 ; Bull.  Denison  Univ.,  vol.  4,  p.  54,  pi.  1,  fig.  6. 

minuscula  Hall.  (See  Cyphaspis  minuscula.) 

missouriensis  Shumard,  1858 ; Trans.  Acad.  Sci.  St.  Louis,  vol.  1,  p.  220. 

Coal  Measures. 

missouriensis  Herrick,  1887 ; Bull.  Denison  Univ.,  vol.  2,  p.  59. 

missouriensis  Vogdes,  1887;  Annals  New  York  Acad.  Sci.,  vol.  4,  p.  86,  pi.  3, 

figs.  1,  2,  14, 1& 

? ornahis.  (See  Cyphaspis  coronata.) 

[ Griffithides  j Meek  and  Worthen.  (See  Griffithides  portlocki.) 

perannulata  Shumard,  1858;  Trans.  Acad.  Sci.  St.  Louis,  vol.  1,  p.  296,  p).  11, 

fig.  10.  Permian. 

• perannulata  Vogdes,  1887 ; Annals  New  York  Acad.  Sci.,  vol.  4,  p.  84. 

praecursor  Herrick,  1888;  Bull.  Denison  Univ.,  vol.  3,  p.  29,  pi.  12,  fig.  1. 

Kinderhook. 

praecursor  Herrick,  1890 ; American  Geologist,  vol.  5,  p.  254. 

[ Proetus ] praecursor  Herrick,  1889;  Bull.  Denison  Univ.,  vol.  4,  p.  54,  pi.  1, 

fig.  1.  Waverly. 

rockfordensis  Winchell,  1865;  Proc.  Acad.  Nat.  Sci.  Phila.,  2d  series,  vol.  9,  p. 

133.  Kinderhook. 

rockfordensis  Herrick,  1887 ; Bull.  Deuison  Univ.,  vol.  2,  p.  62. 

rockfordensis  Vogdes,  1887;  Annals  New  York  Acad.  Sci.,  vol.  4,  p.  91. 

sampsoni  Vogdes,  1888;  Trans.  New  York  Acad.  Sci.,  vol.  7,  p.  248,  figure. 

Waverly.. 

[ Griffithides ] sangamonensis  Meek  anu  Worthen.  (See  Griffithides  sangamo- 

nensis. ) 

[ Griffithides']  scitula  Meek  and  Worthen.  (See  Griffithides  scitula.) 

- — serraticaudata  Herrick,  1889;  Bull.  Denison  Univ.,  vol.  4,  p.  52,  pi.  1,  figs.  8 
a-d.  Keokuk. 

serraticaudata  Herrick,  1890;  American  Geologist,  vol.  5,  p.  254. 

shumardi.  (See  Proetus  auriculata.) 

stevensoni  Meek,  1871 ; Rept.  Regents  Univ.  West  Virginia,  p.  73.  Chester. 

stevensoni  Vogdes,  1887  ; Annals  New  York  Acad.  Sci.,  vol.  4,  p.  88,  pi.  3,  fig.  6. 

tuberculata  Meek  and  Worthen,  1870;  Proc.  Acad.  Nat.  Sci.  Phila.,  p.  52. 

Burlington. 

tuberculata  Vogdes,  1887 ; Annals  New  York  Acad.  Sci.,  vol.  4,  p.  92. 

trinucleata  Herrick,  1887 ; Bull.  Denison  Univ.,  vol.  2,  p.  64,  pi.  1,  figs.  23, 23  a, 

c,  e,  h;  pi.  2,  fig.  32;  pi.  3,  fig.  21.  Coal  Measures. 


V0GOER.] 


CATALOGUE  OF  TRILOBITES. 


135 


Phillipsia  trinucleata  Herrick,  1889;  Bull.  Denison  Univ.,  vol.  4,  p.  49. 

Syn.,  Proetus  trinucleatus  Vogdes,  1888;  Annals  New  York  Acad.  Sci.,  vol.  4,  p. 
(in  error),  pi.  2,  figs.  7,8,9. 

vindobonensis  Hartt,  1868;  Acadian  Geology,  p.  353.  Carboniferous. 

vindobonensis  Herrick,  1887;  Bull.  Denison  Univ.,  vol.  2,  p.  63. 

vindobonensis  Vogdes,  1887 ; Annals  New  York  Acad.  Sci.,  vol.  4,  p.  89.  (See 

Phillipsia  meramecansis  Sbumard.) 

Piliolites  Cozzens,  1846;  Annals  Lyceum  Nat.  Hist.  New  York,  vol.  4,  p.  157. 

oliioensis  Cozzens,  1846;  Annals  Lyceum  Nat.  Hist.  New  York,  vol.  4,  p.  157, 

pi.  16,  figs.  1 a,  1 b.  (See  Proetus  crassimarginatus  ?) 

Proetus  Steininger,  1831 ; M6m.  Soc.  G6ol.  France,  vol.  1,  p.  355,  pi.  24,  fig.  6. 

Type,  Proetus  cuvieri  Steininger. 

Syn.,  PEonia  Burmeister,  1843;  Organization  Trilobites,  p.  116  (Ray  Soci  ed.,  p. 

100).  Burmeister  separates  Dalman’s  species  Calymene  concinna  from  the 
type  of  the  genus  Proetus , and  gives  a generic  description  of  JEonia,  with 
descriptions  and  figures  of  A.  concinna , A.  stolcesii,  and  A.  verticalis. 

Phceton  Barrande,  1846;  Notice  Prelim.,  p.  62.  The  author  hereiu  gives  the 
new  generic  term  Phceton  for  species  of  Proetus  with  fimbriated  pygidia. 

Prinopeltis  Corda,  1847 ; Prodr.,  p.  121.  New  generic  name  proposed  for 
the  preoccupied  term  of  Phceton. 

Xiphogonium  Corda,  1847 ; Prodr.,  p.  70.  Proposed  genus  for  certain  species 
of  Proetus,  with  nine  segments  in  the  thorax. 

Goniopleura.  Corda,  1847;  Prodr.,  p.  80.  This  genus  includes  such  species 
as  Proetus  elegantulus  Loven,  with  twelve  segments  in  the  thorax. 

Forbesia  McCoy,  1847 ; Sil.  Foss.  Ireland,  p.  46.  This  author  uses  for  the 
types  of  his  genus  Forbesia  latifrons  and  F.  stolcesii,  which  is  the  same  as 
that  used  by  Barrande  in  1846  for  his  genus  Phceton  and  Angelin  in  1878 
for  the  genus  Phcethonides. 

Gerastos  Goldfuss,  1843  ; Neues  Jahrbucli  fii.r  Mineral.,  p.  557.  This  genus 
is  a Proetus  with  G.  Icevigatus  for  its  type,  a species  identical  with  Proetus 
cuvieri  Stein. 

Trigonaspis  and  Cylindraspis  the  Brothers  Sanderberger ; Verst,  d.  Rhein, 
Scht.-Syst.,  p.  30,  pi.  3,  1850. 

Dechenella  Kayser,  1880;  Zeitschr.  Deutsch.  geol.  Gesell.,  Berlin,  1880,  p. 
703.  For  such  species  as  Proetus  verticallis  and  P.  halclemani. 

alaricus  Billings,  1860;  Canadian  Naturalist,  vol.  5,  p.  68,  fig.  12.  Hudson. 

alaricus  Billings,  1863;  Geol.  Canada,  p.  219,  fig.  230. 

angustifrons  Hall,  1861 ; Des.  New  Species  Foss.,  p.  70.  Schoharie. 

angustifrons  Hall,  1862;  15th  Rept.  New  York  State  Cab.  Nat.  Hist.,  p.  98. 

angustifrons  Hall,  1876;  Illus.  Devonian  Foss.  Crust.,  pi.  20,  figs.  1,4,7. 

angustifrons  Hall,  1888;  Pal.  New  York,  vol.  7,  n.  91,  pi.  20,  figs.  1-5;  pi.  22, 

figs.  1-3. 

auriculatis.  (See  Proetus  missouriensis  Shumard.) 

canaliculatus  Hall,  1861 ; Des.  New  Species  Foss.,  p.  73.  Upper  Helderberg. 

canaliculatus  Hall,  1862;  15t,h  Rept.  New  York  State  Cab.  Nat.  Hist.,  p.  101. 

canaliculatus  Hall,  1876;  Illus.  Devonian  Foss.  Crust.,  pi.  20,  figs.  10,11. 

canaliculatus  Hall,  1888;  Pal.  New  York,  vol.  7,  p.  107,  pi.  20,  figs.  10,  11;  pi. 

23,  figs.  10, 11. 

clarus  Hall,  1861  ; Des.  New  Species  Foss.,  p.  71.  Upper  Helderberg. 

* clarus  Hall,  1862;  15th  Rept.  New  York  State  Mus.  Nat.  Hist.,  p.  99. 

clarus  Hall,  1876;  Illus.  Devonian  Foss.  Crust.,  pi.  20,  figs.  12-14. 

clarus  Hall,  1888 ; Pal.  New  York,  vol.  7,  p.  104,  pi.  20,  figs.  12-14  ; pi.  22,  figs. 

28-30. 

conradi  Hall,  1861 ; Des.  New  Species  Foss.,  p.  09. 


Schoharie. 


136  A BIBLIOGRAPHY  OF  PALEOZOIC  CRUSTACEA. 


[BULL.  63. 


Pioetus  conradi  Hal],  1862;  15tli  Rept.  New  York  State  Cab.  Nat.  Hist.,  p.  97. 

conradi  Hall,  1876;  Illus.  Devonian  Foss.  Crust.,  pi.  21,  fig.  6 (not  figs.  5,  8,  9); 

pi.  21,  figs.  27, 28. 

Syn.,  Conradi  Hall,  1876;  Illus.  Devonian  Foss.  Crust.,  pi.  2p,  figs.  5,8,9. 

Piliolites  ohionensis?  Cozzens,  1846;  Annals  Lyceum  Nat.  Hist.  New  York, 
vol.  7,  p.  99,  pi.  10,  figs.  1 a,  b. 

conradi  Hall  and  Clarke,  1888 ; Pal.  New  York,  vol.  7,  p.  89,  pi.  20,  fig.  9 ; nl. 

21,  figs.  27,28;  pi.  12,  fig.  4. 

\_Asaphus']  corycceus  Conrad,  1842;  Jour.  Acad.  Nat.  Sci.  Phila.,  vol.  8,  p.  277, 

pi.  16,  fig.  15.  Niagara. 

[ Asaphus ] corycceus  Hall,  1843  ; Geol.  New  York,  4th  Geol  Dist,  pi.  19,  fig.  3. 

corycceus  Hall,  1852;  Pal.  New  York,  vol.  2,  p.  315,  pi.  67,  fig.  15. 

[ Calymene ] crassimarginatus  Hall,  1843;  Geol.  New  York,  4th  Geol.  Dist.,  p. 

172,  fig.  5.  Upper  Helderberg. 

crassimarginatus  Hall,  1859  ; 12th  Rept.  New  York  State  Cab.  Nat.  Hist.,  p.  88. 

[ Pkillipsia ] crassimarginatus  Billings,  1861 ; Canadian  Journal,  vol.  vi,  p.  362. 

crassimarginatus  Hall,  1861 ; Des.  New  Species  Foss.,  p.  72. 

crassimarginatus  Hall,  1862;  15th  Rept.  New  York  State  Cab.  Nat.  Hist.,  p. 

100,  pi.  10,  fig.  10. 

crassimarginatus  Hall,  1876;  Illus.  Devonian  Foss.  Crust.,  pi.  20,  figs.  20-31. 

crassimarginatus  Hall,  1888;  Pal.  New  York,  vol.  7,  p.  99,  pi.  20,  figs.  6-8,  20- 

31;  pi.  22,  figs.  20-62;  pi.  25,  fig.  8. 

curvimarginatus  Hall,  1888  ; Pal.  New  York,  vol.  7,  p.  94,  pi.  22,  figs.  13-19. 

Schoharie. 

davenportensis  Harris.  (See  Froetus  prouti  Shumard.) 

dephinulus  Hail,  1888;  Pal.  New  York,  vol.  7,  p.  Ill,  pi.  23,  figs.  1,  2;  pi.  25, 

fig.  6.  Upper  Helderberg. 

denticulatus  Meek,  1877;  U.  S.  Geol.  Expl.  40th  Par.,  vol.  4,  p.  49,  pi.  1,  figs. 

10  a,  b.  Devonian. 

determinatus  Foerste,  1887 ; Bull.  Denison  Univ.,  vol.  2,  p.  91,  pi.  8,  figs.  2, 3, 3 a. 

Clinton. 

doris  Hall,  1860;  13th  Rept.  New  York  State  Cab.  Nat.  Hist.,  p.  112. 

Goniatite  limestone. 

[ Pkillipsia ] doris  Winchell,  1865 ; Proc.  Acad.  Nat.  Sci.  Phila.,  2d  series,  vol.  2, 

p.  62. 

[Pkillipsia']  doris  Herrick,  1887 ; Bull.  Denison  Univ.,  vol.  2,  p.  62. 

[ Pkillipsia ] doris  Vogdes,  1887;  Annals  New  York  Acad.  Sci.,  vol.  4,  p.  90  (in 

error). 

ellipticus  Meek  and  Worthen,  1865 ; Proc.  Acad.  Nat.  Sci.  Phila.,  p.  267. 

Kinderhook. 

ellipticus  Meek  and  Worthen,  1868;  Geol.  Survey  Illinois,  vol.  3,  p.  460,  pi.  14, 

fig.  3. 

ellipticus  Yogdes,  1887;  AnDals  New  York  Acad.  Sci.,  vol.  4,  p.  82,  pi.  3,  fig.  3. 

folliceps  Hall,  1888  ; Pal.  New  York,  vol.  7,  p.  101,  pi.  23,  figs.  3-8. 

Upper  Helderberg. 

granulatus  Wetherby.  (See  Griffithides  granulatus.) 

haldemani  Hall,  1861;  Des.  New  Species  Foss.,  p.  74.  Hamilton. 

haldemani  Hall,  1862;  15th  Rept.  New  York  State  Cab.  Nat.  Hist.,  p.  102,  pi. 

10,  fig.  6. 

haldemani  Hall,  1876;  Illus.  Devonian  Foss.  Crust.,  pi.  21,  figs.  7-9. 

haldemani  Walcott,  1884 ; Pal.  Eureka  Dist.,  Mon.  U.  S.  Geol.  Survey,  vol.  8, 

p.  210. 

haldemani  Herrick,  1889 ; Bull.  Denison  Univ.,  vol.  4,  p.  55,  pi.  1,  fig.  12. 

haldemani  Hall,  1888  ; Pal.  New  York,  vol.  7,  p.  113,  pi.  21,  figs.  7-9;  pi.  23,  figs. 

13-15. 


vogdes.]  CATALOGUE  OF  TRILOBITES.  137 

Proetus  [Dechenella]  haldemani  Kayser,  1880;  Zeitscbr.  Deutsch.  geol.  Gesell.,  Ber- 
liu,  1880,  p.  770,  pi.  27,  fig.  9. 

[ Dechenella ] haldemani  Tscliernyschew,  1887 ; M6m.  Comity  G6ol.,  vol.  3,  No.  3, 

p.  14,  pi.  1,  fig.  9. 

hesione  Hall,  1861 ; Des.  New  Species  Foss.,  p.  70.  Schoharie. 

hesione  Hall,  1862;  15th  Kept.  New  York  State  Cab.  Nat.  Hist.,  p.  98. 

- — hesione  Hall,  1876;  Illus.  Devonian  Foss.  Crust.,  pi.  20,  figs.  15,  16. 

hesione  Hall,  1888;  Pal.  New  York,  vol.  7,  p.  93,  pi.  20,  figs.  15,  16. 

jejunus.Hall,  1888;  Pal.  New  York,  vol.  7,  p.  124,  pi.  25,  fig.  7.  Hamilton. 

— — junius  Billings,  1863  ; Proe.  Portland  Soc.  Nat.  Hist.,  vol.  1,  p.  122,  pi.  1,  fig.  23. 

Upper  Silurian. 

latimarginatus  Hall,  1888;  Pal.  New  York,  vol.  7,  p.  97,  pi.  22,  figs.  7-12. 

Schoharie. 

loganensis  Hall  and  Whitfield,  1877;  U.  S.  Geol.  Expl.,  40th  Par.,  vol.  4,  p. 

264,  pi.  4,  fig.  33.  Waverly. 

loganensis  Vogdes,  1887 ; Annals  New  York  Acad.  Sci.,  vol.  4,  p.  78. 

longicaudus  Hall,  1861 ; Des.  New  Species  Foss.,  p.  80.  Hamilton. 

longicaudus  Hall,  1862;  15th  Kept.  New  York  State  Cab.  Nat.  Hist.,  p.  108, 

pi.  10,  figs.  7-9. 

longicaudus  Hall,  1876 ; Illus.  Devonian  Foss.  Crust.,  pi.  20,  figs.  32-34. 

longicaudus  Williams,  1881 ; Am.  Jour  Sci.,  3d  series,  vol.  21,  p.  156. 

(?)  longicaudus  Hall,  1888;  Pal.  New  York,  vol.  7,  p.  131,  pi.  20.  figs.  32-34. 

macrobius  Billings,  1863;  Proc.  Portland  Soc.  Nat.  Hist.,  vol.  1,  p.  123,  pi.  1, 

fig.  24.  Upper  Silurian. 

macrocephalus  Hall,  1861 ; Des.  New  Species  Foss.,  pp.  77, 79.  Hamilton. 

macrocephalus  Hall,  1862;  15th  Kept.  New  York  State  Cab.  Nat.  Hist.,  pp. 

105, 107. 

macrocephalus  Hall,  1876 ; Illus.  Devonian  Foss.  Crust.,  pi.  21,  figs.  10-21. 

macrocephalus  Hall,  1888;  Pal.  New  York,  vol.  7,  p.  116,  pi.  21,  figs.  10-21 ; pi. 

23,  fig.  30. 

[Calymene]  marginalis  Conrad,  1839;  Ann.  Rept.  Pal.  Dept.  New  York  Geol. 

Survey,  p.  66.  Tully  Limestone. 

marginalis  Hall,  1861 ; Des.  New  Species  Foss.,  p.  76.  Hamilton. 

marginalis  Hall,  1862;  15th  Rept.  New  York  State  Cab.  Nat.  Hist.,  p.  104. 

marginalis  Hall,  1876;  Illus.  Devonian  Foss.  Crust.,  pi.  21,  figs.  24-28. 

marginalis  Walcott,  1884;  Pal.  Eureka  Dist.,  Mon.  U.  S.  Geol.  Survey,  vol.  8, 

p.  210. 

marginalis  Hall,  1888 ; Pal.  New  York,  vol.  7,  p.  122. 

• microgemma  Hall,  1888  ; Pal.  New  York,  vol.  7,  p.  109,  pi.  22,  figs.  33, 34. 

Upper  Helderberg. 

minuscula  Hall,  1876;  Illus.  Devonian  Foss.  Crust.,  pi.  20,  fig.  17. 

minutus  Herrick,  1889;  Bull.  Denison  Univ.,  vol.  4,  p.  56,  pi.  l,figs.  7 a,  b. 

Kinderliook. 

minutus  Herrick,  1890 ; American  Geologist,  vol.  5,  p.  254. 

missouriensis  Shumard,  1855;  1st  and  2d  Rept.  Geol.  Missouri,  p.  196,  pi.  B, 

figs.  13  a,  b.  Waverly. 

Syn.,  auriculatus  Hall,  1861 ; Des.  New  Species  Foss.,  p.  79. 

auriculatus  Hall,  1862;  15th  Rept.  New  York  State  Cab.  Nat.  Ilist.,  p.  107. 
[ Phillipsia  (Proetus)]  auriculatus  Herrick,  1889;  Bull.  Denison  Univ.,  vol. 
4,  p.  34,  pi.  1,  fig.  14. 

[ Phillipsia ] shumardi  Herrick,  1887 ; Bull.  Denison  Univ.,  vol.  2,  pp.  58, 69, 
pi.  7,  fig.  14. 

missouriensis  Vogdes,  1887;  Annals  Now  York  Acad.  Sci.,  vol.  4,  p.  75,  pi.  3, 

tig.  1. 

missouriensis  Hall,  1888;  Pal.  New  York,  vol.  7,  p.  133,  pi.  23,  fig.  32. 


138  • A BIBLIOGRAPHY  OF  PALEOZOIC  CRUSTACEA.  [BULL. 63. 

Proetus  occidens  Hall,  1861 ; Des.  New  Species  Foss.,  p.  80.  Hamilton. 

occidens  Hall,  1862;  15th  Rept.  New  York  State  Cab.  Nat.  Hist.,  p.  108. 

occidens  Hall,  1876;  Illus.  Devonian  Foss.  Crust.,  pi.  21,  figs.  22,23. 

occidens  Hall.  1888;  Pal.  New  York,  vol.  7,  p.  130,  pi.  21,  figs.  22,23. 

ovifrons  Hall,  16b8;  Pal.  New  York,  vol.  7,  p.  110,  pi.  22,  figs.  31,  32. 

Upper  Helderberg. 

— — pachydermatus  Barrett,  1873;  Am.  Jour.  Sci.,  3d  series,  vol.  15,  p.  370. 

Niagara. 

— — parviusculus  Hall,  1872  ; 24th  Rept.  New  York  State  Cab.  Nat.  Hist.,  p.  223,  pi. 
8,  fig.  14.  Hudson. 

parviusculus  Hall  and  Whitfield,  1875;  Pal.  Ohio,  vol.  2,  p.  109,  pi.  4,  fig.  18. 

parviusculus  Miller,  1874;  Cincinnati  Quart.  Jour.  Sci.,  vol.  1,  p.  144. 

- — peroccidens  Hall  and  Whitfield,  1877  ; U.  S.  Geol.  Expl.  40th  Par. , Pal. , vol.  4, 
p.  262,  pi.  4,  figs.  28-32.  Waverly. 

peroccidens  Vogdes,  1887 ; Annals  New  York  Acad.  Sci.,  vol.  4,  p.  79. 

phocion  Billings,  1874;  Pal.  Foss.,  vol.  2,  p.  63,  fig.  31.  Devonian. 

phocion  Hall,  1888;  Pal.  New  York,  vol.  7,  p.  125,  pi.  25,.  figs.  9,10. 

planimarginatus  Meek,  1871 ; Proc.  Acad.  Nat.  Sci.  Pliila.,  p.  89.  Corniferous. 

planimarginatus  Meek,  1873 ; Pal.  Ohio,  vol.  1,  p.  233,  pi.  23,  figs.  3 a,  b. 

planimarginatus  Hall,  1888;  Pal.  New  York,  vol.  7,  p.  112,  pi.  23,  fig.  12. 

protuberans  Hall,  1859;  Pal.  New  York,  vol.  3,  p.  351,  pi.  73,  figs.  5-8. 

Lower  Helderberg. 

— — prouti  Shumard,  1863;  Trans.  Acad.  Sci.  St.  Louis,  vol.  2,  p.  110.  Hamilton. 
Syn.,  davenportensis  Barris,  1878;  Proc.  Davenport  Acad.  Sci.,  vol.  2,  p.  287,  pi. 
11,  fig.  8. (pi.  11,  fig.  8,  revised). 

prouti  Hall,  1888;  Pal.  New  York,  vol.  7,  p.  126,  pi.  23,  figs.  16-18. 

[ Calymene~\  rowi  Le  Row,  1837 ; Poughkeepsie  Telegram,  Nov.  22.  Hamilton. 

[ Calymeno ] rowi  Green,  1838;  Am.  Jour.  Sci.,  1st  series,  vol.  33,  p.  406. 

■ [ Calymene ] rowi  Green,  1838;  AnnalsMag.  Nat.  Hist.,  1st  series,  London,  vol.  1, 

p.  79. 

rowi  Hall,  1861 ; Des.  New  Species  Foss.,  p.  75. 

rowi  Hall,  1862;  15th  Rept.  New  York  State  Cab.  Nat.  Hist.,  p.  103. 

rowi  Hall,  1876;  Illus.  Devonian  Foss.  Crust.,  pi.  21,  figs.  2-6. 

rowi  Hall,  1888;  Pal.  New  York,  vol.  7,  p.  119,  pi.  21,  figs.  2-6,  24-26;  pi.  23, 

figs.  20-29. 

[ Phillipsia ] shumardi  Herrick,  1887;  Bull.  Denison  Univ.,  vol.  2,  pp.  58,69,  pi. 

7,  figs.  14  a,  b.  Waverly. 

[ Phillipsia ] shumardi  Herrick,  1888;  Bull.  Denison  Univ.,  vol.  3,  p.  29. 

spurlocki  Meek,  1872;  Am.  Jour.  Sci.,  3d  series,  vol.  3,  p.  426.  Hamilton. 

spurlocki  Meek,  1873;  Pal.  Ohio,  vol.  1,  p.  161,  pi.  14,  fig.  12. 

spurlocki  Miller,  1874 ; Cincinnati  Quart.  Jour.  Sci.,  vol.  1,  p.  145. 

stenopyge  Hall,  1888 ; Pal.  New  York,  vol.  7,  p.  110,  pi.  22,  fig.  27. 

Upper  Helderberg. 

stokesi  (Mureh.)  Hall,  1852;  Pal.  New  York,  vol.  2,  p.  316,  pi.  67,  figs.  13, 14. 

Niagara. 

swallowi  Shumard,  1855;  1st  and  2d  Rept.  Geol.  Survey  Missouri,  p.  196,  pi.  B, 

figs.  12  a,  b.  Waverly. 

[ Phillipsia ] swallowi  Herrick,  1887 ; Bull.  Denison  Univ.,  vol.  2,  p.  58. 

[ Phillipsia ] tennesseensis  Winchell,  1869;  Geol.  Tennessee,  p.  445.  Waverly. 

tennesseensis  Vogdes,  1887 ; Annals  New  York  Acad.  Sci.,  vol.  4,  p.  80.  ‘ 

tumidus  Hall,  1888;  Pal.  New  York,  vol.  7,  p.  113,  pi.  23,  fig.  9. 

Upper  Helderberg. 

verneuilli  Hall,  1861 ; Des.  Now  Species  Foss.,  p.  73.  Upper  Helderberg. 

verneuilli  Hall,  1862;  15th  Rept.  New  York  State  Cab.  Nat.  Hist.,  p.  101. 

verneuilli  Hall,  1876;  Illus.  Devonian  Foss.  Crust.,  p.  20,  figs.  18, 19. 


139 


vogdes.  j CATALOGUE  OF  TKILOBITES. 

Proetus  verneuilli  Hall,  1888;  Pal.  New  York,  vol.  7,  p.  108,  pi.  20,  figs.  18, 19. 
Protichnites  Owen,  1852;  Quart.  Jour.  Geol.  Soc.  London,  vol.  8,  p.  214. 

alternans  Owen,  1852;  Quart.  Jour.  Geol.  Soc.  London,  vol.  8,  p.  221,  pi.  8 a, 

7.  Potsdam. 

carbonarius  Dawson,  1873;  Am.  Jour.  Sci.,  3d  series,  vol.  5.  Coal  Measures. 

latus  Owen,  1852;  Quart.  Jour.  Geol.  Soc.  London,  vol.  8,  p.  218,  pi.  11. 

Potsdam. 

- — lineatus  Owen,  1852;  Quart.  Jour.  Geol.  Soc.  London,  vol.  8,  p.  220,  pi.  8 a, 
Pi*  Potsdam. 

logananus  Marsh,  1869;  Am.  Jour.  Sci.,  2d  series,  vol.  48,  p.  46.  Potsdam. 

multinotatus  Owen,  1852;  Quart.  Jour.  Geol.  Soc.  London,  vol.  8,  p.  219,  pi.  12. 

Potsdam. 

octo-notatus  Owen,  1852;  Quart.  Jour.  Geol.  Soc.  London,  vol.  8,  p.  217,  pi.  10. 

Potsdam. 

septem-notatus  Owen,  1852 ; Quart.  Jour.  Geol.  Soc.  London,  vol.  8,  p.  214,  pi.  9. 

Potsdam. 

Protypus  Walcott,  1886;  Bull.  U.  S.  Geol.  Survey,  No.  30,  p.  211. 

[ Angelina ] hitchcocki  Whitfield,  1884;  Bull.  Am.  Mus.  Nat.  Hist.,  New  York, 

vol.  1,  p.  148,  pi.  14,  fig.  13.  Potsdam. 

hitchcocki  Walcott  1886 ; Bull.  U.  S.  Geol.  Survey,  No.  30,  p.  211,  pi.  31,  fig.  4. 

[Bathy  unis']  senectus  Billings,  1861 ; Geol.  Vermont,  vol.  2,  p.  953,  figs.  359,  360. 

Middle  Cambrian. 

[Bathyurus]  senectus  Billings,  1861;  Pamphlet  published  in  adv.  Pal.  Foss. 

Canada,  p.  15,  figs.  20,  21. 

[ Bathijurus ] senectus  Billings,  1863;  Geol.  Canada,  p.  286,  figs.  298  a,b. 

[ Bathijurus ] senectus  Billings,  1865;  Pal.  Foss.,  vol.  1,  p.  15,  figs.  20,21. 

senectus  Walcott,  1886  ; Bull.  U.  S.  Geol.  Survey,  No.  30,  p.  213,  pi.  31,  figs.  2, 

2 a-c. 


Pterocephalia  Roemer,  1852 ; Kreid.  von  Texas,  p.  93. 

[Conocephalites  (Pterocephalia)}  laticeps  Hall  and  Whitfield.  1877;  U.  S.  Geol. 

Expl.  40th  Par.,  vol.  4,  p.  221,  pi.  2,  figs.  4-7.  Potsdam. 

IPtyclioparia  ( Pterocephalia )]  laticeps  Walcott,  1884;  Pal.  Eureka  Dist.,  Mon. 

U.  S.  Geol.  Survey,  vol.  8,  p.  69. 

IPtyclioparia  (Ptwocephalia)']  occidens  Walcott,  1884;  Pal.  Eureka  Dist.,  Mon. 

U.  S.  Geol.  Survey,  vol.  8,  p.  58,  pi.  9,  fig.  21.  Cambrian. 

sancti-sabae  Roemer,  1849;  Texas,  p.  421.  Potsdam. 

sancti-sabae  Roemer,  1852;  Kreid.  von  Texas,  p.  93,  pi.  11. 

Ptychaspis  Hall,  1863;  16th  Rept.  New  York  State  Cab.  Nat.  Hist.,  p.  170. 

Type,  Ptychaspis  miniscaensis  Hall. 

barabuensis  Winchell,  1864;  Am.  Jour.  Sci.,  2d  series,  vol.  37,  p.  230.  Potsdam. 

[ Arionellus ] cylindricus  Billings,  1865;  Pal.  Foss.,  vol.  1,  p.  406,  fig.  385. 

IConoceph.  ( Ptychaspis ?)]  explanatus  Whitfield,  1880;  Ann.  Rept.  Geol.  Survey 

Wisconsin,  1879,  p.  48.  Potsdam. 

\_Conoceph.  ( Ptychaspis ?)]  explanatus  Whitfield,  1882;  Geol.  Wisconsin,  vol.  4, 

p.  181,  pi.  1,  figs.  27,  28. 

Syn granulosa  Hall,  1863;  16th  Rept.  New  York  State  Cab.  Nat.  Hist.,  p.  173 
pi.  6,  figs.  33-4 ). 

granulosa  Whitfield,  1878;  Ann.  Rept.  Geol.  Survey  Wisconsin,  1877,  p.  34. 
granulosa  Whitfield,  18-42;  Geol.  Wisconsin,  vol.  4,  p.  185,  pi.  1,  fig.  24. 

In  this  work  Ptychaspis  granulosa  Hall  (not  Owen)  is  referred  to  Ptychaspis 
striata. 

granulosa  Whitfield,  1882;  Geol.  Wisconsin,  vol.  4,  p.  185,  pi.  1,  fig.  24. 

Syn.,  Dikeloccphalus  miniscaensis  Owen,  1852;  Rept.  Geol.  Survey  Wisconsin, 
Iowa,  and  Minnesota,  p.  574,  pi.  1,  figs.  3, 12  ; pi.  I a,  figs.  4. 5. 

iDikelocephalus-)  granulosus  Owen,  1852;*  Rept.  Geol.  Survey  Wisconsin,  Iowa 

and  Minnesota,  p.  575,  pi.  1,  fig.  7.  Potsdam. 


[bull.  G3. 


140  A BIBLIOGRAPHY  OF  PALEOZOIC  CRUSTACEA. 

Ptychaspis  miniscaensis  Hall,  1863;  lGfcli  Kept.  New  York  State  Cab.  Nat.  Hist.,  p. 
171,  pi.  6,  figs.  41-46;  pi.  10,  figs.  21 , 22. 

minuta  Whitfield,  1878;  Aun.  Kept.  Geol.  Survey  Wisconsin,  1877,  p.  55. 

Potsdam. 

minuta  Whitfield,  1882  ; Geol.  Wisconsin,  vol.  4,  p.  186,  pi.  1,  figs.  25, 26. 

minuta  Walcott,  1884 ; Pal.  Eureka  Dist.,  Mon.  U.  Geol.  Survey,  vol.  8,  p.  60,  pi. 

10,  fig.  23. 

pustulosa  Hall  and  Whitfield,  1877;  U.  S.  Geol.  Expl.  40th  Par.,  Pakeont.,  vol. 

4,  p.  223,  pi.  2,  fig.  27.  Potsdam. 

[lHkeloceplialus ] sesostris  Billings,  1865;  Pal.  Foss.,  vol.  1,  p.  198,  fig.  184. 

Quebec. 

speciosus  Walcott,  1879;  32d  Rept.  New  York  State  Mus.  Nat.  Hist.,  p.  131. 

Calciferous. 

striata  Whitfield,  1878;  Ann.  Rept.  Geol.  Survey  Wisconsin,  1877,  p.  55.  * 

Potsdam. 

striata  Whitfield,  1880;  Ann.  Rept.  Geol.  Survey  Wisconsin,  1879,  p.  51. 

striata  Whitfield,  1882 ; Geol.  Wisconsin,  vol.  4,  p.  186. 

Syn.,  granulosa  Hall,  1863;  16th  Rept.  New  York  State  Cab.  Nat.  Hist.,  p.  173, 
pi.  6,  figs.  33-40. 

[ Arionellus]  subclavatus  Billiugs,  1860;  Canadian  Naturalist,  vol.  5,  p.  315, 

figs.  15, 15  a.  Quebec. 

Ptychoparia  Corda,  1847 ; Prodr.,  p.  141,  pi.  2,  fig.  11. 

Type,  Ptychoparia  striatus  Emmrich. 

[ Conocephalites ] adamsi  Billings,  1861 ; Pamphlet  published  in  adv.  Pal.  Foss., 

p.  12,  figure.  * 

[ Conoceplialus']  Adams,  1848;  Am.  Jour.  Sci.,  2d  series,  vol.  5,  p.  109. 

[ Conocephalites ] adamsi  Billings,  1861 ; Geol.  Vermont,  vol.  2,  p.  950,  fig.  355.- 

[ Conoceplialus ] Billings,  1861;  Am.  Jour  Sci.,  2d  series,  vol.  32,  p.  231. 

[ Conoceplialus ] Billings,  1861;  Canadian  Naturalist,  vol.  6,  p.  324. 

[ Conocephalites ] adamsi  Billings,  1863;  Geol.  Canada,  p.  286,  lig.  294. 

[Conocephalites]  adamsi  Billings,  1865;  Pal.  Foss.,  vol.  1,  p.  12,  fig.  15. 

adamsi  Walcott,  1886;  Bull.  U.  S.  Geol.  Survey,  No.  30,  p.  195,  pi.  26,  figs.  1, 

1 a-c.  Middle  Cambrian. 

Syn.,  arenosus  (Billings)  Walcott,  1886;  Bull.  U.  S.  Geol.  Survey,  No.  30,  p.  195. 

[ Eulomaf ] aflinis  Walcott,  1882;  Pal.  Eureka  Dist.,  Mon.  U.  S.  Geol.  Survey, 

vol.  8,  p.  54,  pi.  10,  fig.  12.  Cambrian  and  Silurian. 

[Crepicephalus  (Bath yarns)]  angulatus  Hall  and  Whitfield,  1877;  U.  S.  Geol. 

Expl.  40th  Par.,  Palseont.,  vol.  4,  p.  220,  pi.  2,  fig.  28.  Potsdam. 

? angulatus  Walcott,  1884;  Pal.  Eureka  Dist.,  Mon.  U.  S.  Geol.  Survey,  vol.  8, 

p.  269. 

? annectans  Walcott,  1884 ; Pal.  Eureka  Dist.,  Mon.  U.  S.  Geol.  Survey,  vol.  8, 

p.  91,  pi.  12,  fig.  18.  Cambrian. 

[ Crepicephalus  (Loganellus)]  anytus  Hall  and  Whitfield,  1877;  U.  S.  Geol.  Expl. 

40th  Par.  vol.  4,  p.  219,  pi.  2,  figs.  19-21.  Potsdam. 

anytus  Walcott,  1884;  Pal.  Eureka  Dist.,  Mon.  U.  S.  Geol.  Survey,  vol.  8,  p.  56, 

pi.  9,  fig.  26. 

[ Lisostracus ] anytus  Brogger,  1886;  Geol.  Foren.  Stock.  Forhandl.,  vol.  8,  p.  212. 

[Conoceph.]  antiquatus  Salter,  1859;  Quart.  Jour.  Geol.  Soc.  London,  vol.  15,  p. 

554,  fig.  2.  Potsdam. 

Syn.,  [Conoceph.  ~)  arenosus  Billings,  1861 ; Geol.  Vermont,  vol.  2,  p.  952,  fig.  358. 

[ Conoceph.  ] arenosus  Billings,  1861;  Pamphlet  published  in  advance  of  Pal. 

Foss.  Canada,  vol.  1 ; also,  Pal.  Foss.,  vol.  1,  p.  15,  fig.  18. 

[Conoceph.  J arenosus  Billings,  1863;  Geol.  Canada,  p.  286,  fig.  297. 

Walcott  (Bull.  U.  S.  Geol.  Survey,  No.  30,  p.  195)  refers  this  species  to  Pty- 
choparia adamsi. 


vogdes.  ] CATALOGUE  OF  TRILOB1TES.  141 

Ptychoparia  [ Conoceph . ] aurora  Hartt,  1868  ; Acadian  Geology,  p.  653.  (See  Ptycho- 
paria  ouangondianus.) 

[ Conoceph .]  billingsi  Shumard,  1861 ; Am.  Jour.  Sci.,  2d  series,  vol.  32,  p.  219. 

Potsdam. 

[Conoceph.  f]  binodosus  Hall,  1863;  16th  Rept.  New  York  State  Cab.  Nat.  Hist., 

p.  16U,  pi.  7,  fig.  47.  Potsdam. 

[Solenopleura  f ] breviceps  Walcott,  1884;  Pal.  Eureka  Dist.,  Mon.  U.  S.  Geol. 

Survey,  vol.  8,  p.  49,  pi.  10,  fig.  9.  Cambrian. 

[Conocephalites]  calymenoides  Whitfield,  1878;  Ann.  Rept.  Geol.  Survey  Wis- 
consin, 1877,  p.  52.  Potsdam. 

[ Conocephalites ] calymenoides  Whitfield,  1882;  Geol.  Wisconsin,  vol.  4,  p.  179, 

pi.  3,  figs.  2-5. 

calymenoides  Walcott,  1884 ; Pal.  Eureka  Dist.,  Mon.  U.  S.  Geol.  Survey,  vol. 

8,  p.  48. 

[Crepicephalus  ( Loganellus )]  centralis  Whitfield,  1880 ; Geol.  Resources  Black 

Hills  Dakota,  p.  341,  pi.  2,  figs.  21-24.  Potsdam. 

[Conocephalites]  chippewaensis  (Owen)  Shumard,  1863;  Trans.  St.  Louis  Acad. 

Sci.,  vol.  2,  p.  104. 

[ Lonchocephalus ] chippewaensis  Owen,  1852;  Rept.  Geol.  Survey  Wisconsin, 

Iowa,  and  Minnesota,  p.  576,  pi.  8,  figs.  6,  14 ; pi.  1 a,  fig.  9. 

? (subgenus  ?)  clavata  Walcott,  1887 ; Am.  Jour.  Sci.,  3d  series,  vol.  34,  p.  198, 

pi.  1,  fig.  3.  * Cambrian. 

[ Conoceph ] cordillerae  Rominger,  1887  ; Proc.  Acad.  Nat.  Sci.  Pliila.,  p.  17,  pi.  1, 

fig.  7.  Cambrian. 

cordillerae  Walcott,  1888;  Am.  Jour.  Sci.,  3d  series,  vol.  36,  p.  165. 

[Conoceph]  depressus  Shumard,  1861;  Am.  Jour.  Sci.,  2d  series,  vol.  32,  p.  219. 

Potsdam. 

[Conoceph]  diadematus  Hall,  1863;  16th  Rept.  New  York  State  Cab.  Nat.  Hist., 

p.  167,  pi.  7,  figs.  36-39;  pi.  9,  figs.  18-21  (?).  Potsdam. 

[Eulomaf]  dissimilis  Walcott,  1884;  Pal.  Eureka  Dist.,  Mon.  U.  S.  Geol.  Survey, 

vol.  8,  p.  51,  pi.  9,  fig.  28.  Cambrian. 

[Conoc&ph  (Arionellus  ?)]  dorsalis  Hall,  1863;  16th  Rept.  New  York  State  Cab. 

Nat.  Hist.,  p.  222.  • Potsdam. 

[Conoceph]  elegans  Hartt,  1868;  Acadian  Geology,  p.  650,  St.  John. 

[Conoceph]  eos  Hall,  1863;  16th  Rept.  New  York  State  Cab.  Nat.  Hist.,  p.  151, 

pi.  7,  figs.  24,  25;  pi.  8,  figs.  2-9.  Potsdam. 

eos  Walcott,  1884;  Pal.  Eureka  Dist.,  Mon.  U.  S.  Geol.  Survey,  vol.  8,  p.  51. 

[ Conoceph. ] eryon  Hall,  1863 ; 16th  Rept.  New  York  State  Cab.  Nat.  Hist.,  p.  157, 

pi.  7,  figs.  10-16;  pi.  8,  figs.  16,31.  Potsdam. 

fitchi  Walcott,  1887;  Am.  Jour.  Sci.,  3d  sories,  vol.  34,  p.  197,  pi.  1,  fig.  6. 

Cambrian. 

[Conoceph.]  formosm  Hartt.  (See  Ptychoparia  robbi  Hartt.) 

[Conoceph.  ( Ptychoparia )]  gallatinensis  Meek,  1873;  6th  Ann.  Rept.  U.  S.  Geol. 

Survey  Territories,  1872,' p.  485.  Potsdam. 

Referred  by  Walcott  to  Ptychoparia  oweni  Meek  and  Hayden. 

[Crepicephalus  [Loganellus])  granulosus  Hall  and  Whitfield,  1877;  U.  S.  Geol. 

Expl.  40th  Par.,  Palseont.,  vol.  4,  p.  214,  pi.  2,  figs.  1,  2,  3.  Potsdam. 

granulosus  Walcott,  1884  ; Pal.  Eureka  Dist.,  Mon.  U.  S.  Geol.  Survey,  vol.  8, 

p.  57. 

[Crepicephalus  (Loganellus)]  haguei  Hall  and  Whitfield,  1877;  U.  S.  Geol.  Expl. 

40th  Par.,  Pabeont.,  vol.  4,  p.  210,  pi.  2,  figs.  14,  15.  Potsdam. 

haguei  Walcott,  1884 ; Pal.  Eureka  Dist.,  Mon.  U.  S.  Geol.  Survey,  vol.  8,  p.  57. 

[ Lisostracus ] haguei  Brogger,  1886;  Geol.  Foreningens  Stockholm  Forhandl., 

vol.  8,  p.  202. 

[Conoceph.  ] halli  Hartt.  (Sec  Ptychoparia  orestes  Hartt.) 


142 


A BIBLIOGRAPHY  OF  PALEOZOIC . CRUSTACEA., 


[BULL.  63. 


Ptychoparia  housensis  Walcott,  1886;  Bull.  U.  S.  Geol.  Survey,  No.  30,  p.  201,  pi.  25, 
fig.  5.  Middle  Cambrian, 

[Conocoryphe  (Concephalites)]  kingii  Meek,  1870;  Proe.  Acad.  Nat.  Sci.  Pliila., 

vol.  22,  p.  63. 

[Conocoryphe  (Concephalites)]  kingii  Meek,  1877 ; U.  S.  Geol.  Expl.  40th  Par., 

Pakeont.,  vol.  4,  p.  20,  pi.  1,  tig.  4. 

[_  Conocoryphe  ( Ptychoparia )]  kingii  Meek,  1873;  6th  Ann.  Kept.  U.  S.  Geol.  Sur> 

vey  Territories,  1872,  p,  487. 

[Conocoryphe  ( Ptychoparia )]  kingii  White,  1876;  U.  S.  Geog\  and  Geol.  Surveys 

West  100th  Mer.,  Palseont.,  vol.  4,  p.  40,  pi.  2,  tigs.  2 a,  b,  c. 

[Liostracus]  kingii  Brogger,  1^86;  Geol.  Foreningens  Stockholm  Forhandi., 

vol.  8,  p.  205. 

-•  - • kingii  Walcott,  1886 ; Bull.  U.  S.  Geol.  Survey,  No.  30,  p.  193,  pi.  27,  figs.  4,  4 a. 

Middle  Cambrian. 

laeviceps  Walcott,  1884;  Pal.  Eureka  Dist.,  Mon.  U.  S.  Geol.  Survey,  vol.  8,  p. 

54,  pi.  10,  figs.  17,  18.  Cambrian. 

[Conoceplialites  (Pterocephalus)]  laticeps  Hall  and  Whitfield,  1877;  U.  S.  Geol. 

Expl.  40th  Par.,  Pakeont.,  vol.  4,  p.  67,  221,  pi.  2,  figs,  4-7.  Cambrian. 

— — [ Pterocephalus ] laticeps  Walcott,  1884;  Pal.  Eureka  Dist.,  Mon.  U.  S.  Geol.  Sur" 
vey,  vol.  8,  p.  59. 

? linnarssoni  Walcott,  1884;  Pal.  Eureka  Dist.,  Mon.  U.  S.  Geol.  Survey,  vol.  8, 

p.  47,  pi.  9,  figs.  18, 18  a.  • Cambrian. 

[ Loganellus ] logani  Devine,  1863;  Canadian  Naturalist,  vol.  8,  p.  95,  figure. 

Potsdam. 

[ Olenusf  ] logani  Billings,  1865;  Pal.  Foss.,  vol.  1,  p.  201,  figs.  185,  186. 

Syn.,  [ Loganellus']  quebecensis  Billings  ; idem.,  p.  203. 

logani  Walcott,  1884 ; Bull.  U S.  Geol.  Survey,  No.  10,  p.  36. 

[Crepicephalus  {Loganella)]  maculosus  Hall  and  Whitfield,  1877;  U.  S.  Geol. 

Expl.  40th  Par.,  Palseont.,  vol.  4,  p.  215,  pi.  2,  figs.  21,  25,  26(?).  Potsdam. 

maculosus  Walcott,  1884 ; Pal.  Eureka  Dist.,  Mon.  U.  S.  Geol.  Survey,  vol.  8,  pj). 

269,  271. 

[ Conoceph.  ] minor  Shumard,  1863 ; Traus.  Acad.  Nat.  Sci  St.  Louis,  vol.  2,  p.  105. 

Potsdam. 

(Undet.)  tri lob ite  Owen,  1848;  Geol  Recounoissance  Chippewa  Land  Dist.,  p.  15, 

pi.  7,  fig.  4. 

[Conoceph.]  minor  Hall,  1863;  16th  Rept.  New  York  State  Cab.  Nat.  Hist.,  p.  149, 

pi.  8,  figs.  1-4. 

mijior  Walcott,  1884;  Pal.  Eureka  Dist.,  Mon.  U S.  Geol  Survey,  vol.  8,  p.  91. 

[Conoceph.]  minutus  Bradley,  1860;  Am.  Jour.  Sci.,  2d  series,  vol.  30,  p.  24,  3 

figs.  Potsdam. 

[Conoceph.  ] minutus  Bradley,  1860;  Canadian  Naturalist,  vol.  5,  p.  420,  figs.  1-3. 

[ Conoceph. ] minutus  Hall,  1863;  16th  Rept.  New  York  State  Cab.  Nat.  Hist.,  p. 

150,  pi.  8,  figs.  5-7.  . 

minutus  Walcott,  1884 ; Pal.  Eureka  Dist.,  Mon.  U.  S.  Geol.  Survey,  vol.  8,  p.  91. 

minutus  Walcott,  18feS6;  Bull.  U.  S.  Geol.  Survey,  No.  30,  p.  21. 

[Conoceph.]  miser  Billings,  1861 ; New  or  little  known  Sil.  Foss.,  p.  12,  fig.  14. 

Potsdam. 

[Conoceph.]  miser  Billings,  1861 ; Geol.  Vermont,  vol.  2,  p.  950,  fig.  354. 

[ Conoceph. ] miser  Billings,  1863;  Geol.  Canada,  p.  286,  fig.  393. 

[Conoceph.]  miser  Billings,  1865 ; Pal.  Foss.,  vol.  1,  p.  12,  fig.  14. 

miser  Walcott,  1886;  Bull.  U.  S.  Geol  Survey,  No  30,  p.  199,  pi.  27,  fig.  2. 

[Crepicephalus  (Loganella)]  montanensis  Whitfield,  1876;  Rept.  Recon  Upper 

Missouri,  p.  141,  pi.  1,  tigs.  1,  2.  Potsdam. 

montanensis  Walcott,  1884  ; Pal.  Eureka  Dist.,  Mon.  U.  S.  Geol.  Survey,  vol.  8, 

pp.  53,  56, 


V0GDB8.  ] 


CATALOGUE  OF  TRILOBITES. 


143 


Ptychoparia  mucronatus  Shaler  and  Foerste,  1888 ; Bull.  Mus.  Comp.  Zool.  Har- 
vard Coll.,  vol.  16,  p,  37,  pi.  2,  fig.  21.  Cambrian. 

[Conocepli.]  nasutus  Hall,  1863;  16tli  Kept.  New  York  State  Cab.  Nat.  Hist.,  p. 

155,  pi.  7,  figs.  3-9.  Potsdam. 

[ Conocepli .]  neglectus.  (See  Ptychoparia  tener.) 

— — [Crepiceplialus  {Loganella)]  nitidus  Hall  and  Whitfield,  1877;  U.  S.  Geol.  Expl. 
40th  Par.,  Palieont.,  vol.  4,  p.  212,  pi.  2,  figs.  8-10.  Cambrian. 

Syn.,  Crepicephalus  [ Loganella J simulator  (Hall  and  Whitfield)  Walcott. 

nitidus  Walcott,  1884 ; Pal.  Eureka  Dist.,  Mou.  U.  S.  Geol.  Survey,  vol.  8,  p.  57. 

— occidentalis  Walcott,  1884;  Pal.  Eureka  Dist.,  Mon.  U.  S.  Geol.  Survey,  vol.  8, 
p.  51,  pi.  10,  fig.  5.  Cambrian. 

[ Conocepli.  ] orestes  Hartt,  1868;  Acadian  Geology,  p.  649,  fig.  225.  St.  John. 

Syn.,  Conocepli . halli  (Hartt)  Walcott;  Bull.  U.  S.  Geol.  Survey,  No.  10,  p.  40. 

Conocepli.  thersites  (Hartt;  Walcott;  Bull.  U.  S.  Geol.  Survey,  No.  10,  p.  40. 

orestes  var.  thersites  Walcott,  1884 ; Bull.  U.  S.  Geol.  Survey,  No.  10,  p.  40. 

Syn.,  orestes  Walcott,  1884 ; Bull.  U.  S.  Geol.  Survey,  No.  10,  p.  39,  pi.  5,  figs.  3, 
3 a, 

[ Solenopleura]  orestes  Matthew,  1887 ; Trans.  Royal  Soc,  Canada,  vol.  4,  p.  154. 

pi.  2,  figs.  4 a-e. 

[ Pterocephalus ] occidens  Walcott,  1884;  Pal.  Eureka  Dist'.,  Mon.  U.  S.  Geol.  Sur- 
vey, vol.  8,  p.  58,  pi.  9,  fig.  21.  Cambrian. 

[ Conocepli .]  ouangondiana  Hartt,  1868;  Acadian  Geology,  p.  651,  fig.  226. 

St.  John. 

ouangondiana  Walcott,  1884;  Bull.  U.  S.  Geol.  Survey,  No.  10,  p.  37,  pi.  5,  figs. 

4,  4 a-f. 

ouangondiana  var.  aurora  (Hartt)  Walcott;  Bull.  U.  S.  Geol.  Survey,  No.  10, 

p.  38,  pi.  5,  fig.  5. 

[ Liosiracii8 ] ouangondiana  Matthew,  18S7 ; Trans  Royal  Soc.  Canada,  p.  138. 

oweni  (Meek  and  Hayden)  Walcott,  1884  ; Pal.  Eureka  Dist.,  Mon.  U.  S.  Geol. 

Survey,  vol.  8,  p.  55,  pi.  10,  figs.  3,  3 a.  (See  Agraulus  oweni  Meek  and  Hay- 
den.) 

The  following  species  are  referred  by  Walcott  (Mon.  U.  S.  Geol.  Survey,  vol. 
8,  p.  55)  to  Ptychoparia  oweni : 

Arionellus  oweni  Meek  and  Hayden,  1862 ; Am.  Jour.  Sci.,  2d  series,  vol.  33,  p.  74. 
Agraulos  oweni  Meek  and  Hayden,  1864;  Pal.  Upper  Missouri,  p.  9,  figs,  a-c,  pi. 

l.fig-  4- 

Conocoryplie  ( Ptychoparia ) gallatinensis  Meek,  1870;  6tli  Ann.  Rept.  U.  S.  Geol. 
Survey  Territories,  1872,  p.  485. 

Crepicephalus  ( Loganella ) centralis  Whitfield,  1880;  Geol.  Resources  Black  Hills, 
D akota,  p.  341,  pi.  2,  figs.  21-24. 

[ Conocepli . ] oweni  Hull,  1863 ; 16th  Rept.  New  York  State  Cab.  Nat.  Hist.,  p.  155, 

pi.  8,  figs.  17-20.  Potsdam. 

I Crepicephalus  ( Loganella )]  planus  Whitfield,  1877 ; Prelim.  Rept.  Pal.  Black 

Hills,  p.  11.  Potsdam. 

[Crepicephalus]  planus  Whitfield,  1880;  Geol.  Black  Hills  Dakota,  p.  343,  pi.  2, 

fig.  20. 

? pernasutus  Walcott,  1884  ; Pal.  Eureka  Dist.,  Mon.  U.  S.  Geol.  Survey,  vol.  8.  p, 

49,  pi.  10,  figs.  8, 8 a,  b.  Cambrian. 

[Conocepli. ] perseus  Hall,  1863;  16th  Rept.  New  York  State  Cab.  Nat.  Hist.,  p.  153, 

pi.  7,  figs.  17-22 ; pi.  8,  fig.  33.  Potsdam. 

piochensis  Walcott,  1886;  Bull.  U.  S.  Geol.  Survey,  No.  30,  p.  201.pl.  26,  fig.  2- 

2 a,  b ; pi.  28,  figs.  1-1  a-e.  Middle  Cambrian. 

? prospectensis  Walcott,  1884  ; Pal.  Eureka  Dist.,  Mon.  U.  S.  Geol.  Survey,  vol. 

8,  p.  46,  pi.  9,  fig.  20.  Cambrian. 

? prospectensis  Walcott,  1886;  Bull.  U.  S.  Geol.  Survey,  No.  30.  p.  202,  pi.  37, 

fig.  5. 


144  A BIBLIOGRAPHY  OF  PALEOZOIC  CRUSTACEA.  [bull. 63. 

Ptychoparia  quadrangularis  Whitfield.  The  specific  name  of  Conoceph , quadratus 
being  preoccupied,  Prof.  R.  P.  Whitfield  substitutes  that  of  quadrangular  is  for 
the  species. 

[Crepicepalus  ( LoganeUa )]  quadrans  Hall  and  Whitfield,  1877 ; U.  S.  Geol.  Expl. 

40th  Par.,  Palaeont.,  vol.  4,  p.  238,  pi.  2,  figs.  11-13. 

— — quadrans  Walcott,  1886  ; Bull.  U.  S.  Geol.  Survey,  No.  30,  p.  199,  pi.  29,  figs.  4-4 
a,  b.  Cambrian, 

[Conoceph.]  quadratus.  (See  Ptychoparia  quadrangularis.) 

[ Conoceph. ] quadratus  Hartt,  1868;  Acadian  Geology,  p.  654.  St.  John. 

quadratus  Walcott,  1884  ; Bull.  U.  S.  Geol.  Survey,  No.  10;  p.  39,  pi.  5,  fig.  1. 

[Conoceph.  f]  quadratus  Whitfield,  1880;  Ann.Rept.  Geol.  Survey,  Wisconsin, 

1879,  p.  47. 

[Conoceph.  ?]  quadratus  Whitfield,  1882;  Geol.  Wisconsin,  vol.  4,  p 180, pi.  1, 

figs.,  15, 16.  (See  Ptychoparia  quadrangularis  Whitfield.) 

[ Conoceph .]  robbi  Hartt,  1868 ; Acadian  Geology,  p.  648.  St.  John. 

Syn.,  Conoceph.  formosa  (Hartt)  Walcott ; Bull.  U.  S.  Geol.  Survey,  No.  10,  p.  36. 

robbi  Walcott,  1884  ; Bull.  U.  S.  Geol.  Survey,  No.  10,  p.  36,  pi.  6,  figs.  1, 1 a. 

[Solenopleura]  robbi  Matthew,  1887 ; Trans.  Royal  Soc.  Canada,  vol.  4,  p.  153,  pi. 

2,  figs.  3 a-1 ; fig.  4 a-e. 

rogersi  Walcott,  1884 ; Bull.  U.  S.  Geol.  Survey,  No.  10,  p.  47,  pi.  7,  fig.  2. 

Lower  Cambrian. 

[ Conoceph .]  shumardi  Hall,  1863 ; 16th  Kept.  New  York  State  Cab.  Nat.  Hist.,  p. 

154,  pi.  7,  figs.  1-2 ; pi.  3,  figs.  19, 32.  Potsdam. 

similis  Walcott,  1884 ; Pal.  Eureka  Dist.,  Mon.  U.  S.  Geol.  Survey,  vol.  8,  p.  52,  pi. 

10,  figures.  Cambrian. 

similis  var.  rolSustus  Walcott ; idem.,  p.  53,  pi.  1,  figs.  9, 9 a. 

* [Conoceph.]  subcoronatus  Hall  and  Whitfield,  1877;  U.  S.  Geol.  Expl.  40th 

Par.,  Palaeont.,  vol.  4,  p.  237,  pi.  2,  fig.  1. 

subcoronatus  Walcott,  1886;  Bull.  U.  S.  Geol.  Survey,  No.  30,  p.  205,  pi.  28, 

fig.  4.  Middle  Cambrian. 

[ Conoceph.  ] teucer  Billings,  1861;  New  or  little  known  Sil.  Foss.,  p.  12, 

fig.  16. 

[Conoceph.]  teucer  Billings,  1861  ; Geol.  Vermont,  vol.  2,  p.  951,  fig.  356. 

- [Conoceph.]  teucer  Billings,  1865;  Pal.  Foss.,  vol.  1,  p.  13,  fig.  16. 

[Cenoceph.]  teucer  Billings,  1863;  Geol.  Canada,  p.  286,  fig.  295. 

teucer  Walcott,  1886;  Bull.  U.  S.  Geol.  Survey,  No.  30,  p.  197,  pi.  26,  fig.  3. 

Middle  Cambrian. 

[Conoceph.]  tener  Hartt,  1868;  Acadian  Geology,  p.  652.  St.  John. 

Syn.,  Conoceph.  neglectus  (Hartt)  Walcott,  1884;  Bull.  U.  S.  Geol.  Survey,  No.  10, 
p.  41. 

tener  Walcott,  1884  ; Bull.  U.  S.  Geol.  Survey,  No.  10,  p.  41,  pi.  5,  figs.  6,  6 a,  b. 

[Conoceph.]  thersites.  (See  Ptychoparia  orestus  Hartt.) 

trilineatus.  (See  Atops  trilineatus,  Conocoryphe  trilineatus,  Conocepha- 

lites  trilineatus,  Calymene  beckii,  Triarthrus  beckii.) 

[Crepicephalus  ( LoganeUa )]  unisulcatus  Hall  and  Whitfield,  1877;  U.  S.  Geol. 

Expl.  40th  Par.,  Palaeont.,  vol.  4,  p.  216,  pi.  2,  figs.  22,23.  Cambrian. 

unisulcatus  Walcott,  1884  ; Pal.  Eureka  Dist.,  Mon.  U.  S.  Geol.  Survey,  vol.  8, 

p.  58. 

[Conoceph.]  verucosus  Whitfield,  1884  ; Bull  Am.  Mus.  Nat.  Hist.,  vol.  1,  p.  146, 

pi.  14,  fig.  12.  Potsdam. 

[Conoceph.]  vulcanus  Billings,  1861;  New  or  little  known  Sil.  Foss.,  p.  14, 

fig.  17. 

[Conoceph.]  vulcanus  Billings,  1861;  Geol.  Vermont,  vol.  2,  p.  952,  fig.  357. 

[Conoceph  ] vulcanus  Billings,  1863;  Geol.  Canada,  p.  286,  fig.  296. 

[Conoceph.]  vulcanus  Billings,  1865;  Pal.  Foss.,  vol.  1,  p.  14,  fig.  17. 


YOGDES.] 


CATALOGUE  OF  TRILOBITES. 


145 


Ptychoparia  vulcanus  Walcott,  1886;  Bull.  U.  S.  Geol.  Survey,  No.  30,  p.  196,  pi. 
26,  figs.  4,  4 a.  Middle  Cambrian. 

Compare  Ptychoparia  adamsi. 

lConoceph.~\  winona  Hall,  1863;  16th  Rept‘.  New  York  State  Cab.  Nat.  Hist.,  p. 

161,  pi.  7,  figs.  28-28.  Potsdam. 

[ Conocepli.  ] zenkeri  Billings,  1860;  Canadian  Naturalist,  vol.  5,  p.  305,  fig.  4. 

Quebec. 

[ Conoceph .]  zenkeri  Billings,  1865 ; Pal.  Foss.,  vol.  1,  p.  398,  fig.  375. 


Remopleurides  Portlock,  1843;  Rept.  Geol.  Londonderry,  etc.,  p.  254. 

Type,  Remopleurides  colbii  Portlock. 

Syn.,  Caphyra  Barrande,  1846;  Notice  Pr61im.,  p.  32. 

Ampliytryon  Corda,  1847 ; Prodr.,  p.  228. 

affinis  Billings,  1865 ; Pal.  Foss.,  vol.  1,  p.  325,  fig.  313.  Quebec. 

canadensis  Billings,  1865;  Pal.  Foss.,  vol.  1,  p.  182,  fig.  164.  Chazy. 

pander!  Biilings,  1865;  Pal.  Foss.,  vol.  1,  p.  293,  fig.  283.  Quebec. 

? schlotheimi  Billings,  1865;  Pal.  Foss.,  vol.  1,  p.  294,  tig.  284.  Quebec. 

Syn.,  Paradoxides  or  Olenellus  Billings,  1863;  Geol.  Canada,  pp.  871,872. 

striatulus  Walcott,  1875;  Cincinnati  Quart.  Jour.  Sci.,  vol.  2,  p.  347,  fig.  27, 

27  a,  b.  Trenton. 

Sao  Barrande,  1846 ; Notice  Prelim.  Syst.  Sil.  Boheme,  p.  13. 


? lamottensis  Whitfield,  1886;  Bull.  Am.  Mus.  Nat.  Hist.  New  York,  vol.  1,  p. 

334,  pi.  33,  figs.  9-11.  Birdseye  Limestone. 

Shumardia  Billings,  1862;  Pal.  Foss.,  vol.  1,  p.  92. 

Type,  Shumardia  granulosa  Billings. 

The  generic  name  therein  suggested  by  Mr.  E.  Billings  for  a minute  Trilobite 
includes  a specimen  having  an  expanding  glabella,  with  two  anterior  side 
nodules,  simular  to  those  of  Batius  pusillus  Sar,  the  genus  being  allied  to 
Agnostus,  differing  therefrom  in  having  a regularly  ribbed  pygidium,  similar  to 
that  of  an  Asaphus.  Comparing  Mr.  E.  Billings’s  type,  Shumardia  granulosa , 
with  Conophrys  salopiensis  Galloway  (Quart.  Jour.  Geol.  Soc.  London,  vol.  33,  p. 
667,  pi.  12,  fig.  7),  which  W.  C.  Brogger  (Sil.  Etagen  2 und  3,  p.  125)  refers  to  as 
a synonym  to  Battus  pusillus , we  fiod  a similar  characteristic  in  the  glabella. 
The  pygidium  of  Shumardia  granulosa  has  however  a more  semi- oval  form,  with 
a greater  number  of  axis  rings  and  an  additional  number  of  ribs  on  the  side 
lobes. 

The  head  of  Shumardia  granulosa  differs  from  Battus  pusillus  in  having  a 
groove,  which  runs  from  the  anterior  front  of  the  glabella  to  the  frontal  margin 
of  the  head,  a characteristic  of  some  species  of  Agnostidce  ( vid . Brogger,  Sil. 
Etagen  2 und  3,  pi.  1,  fig.  10). 

Mr.  Billings  remarks  “that  in  some  specimens  this  furrow  has  at  the  bottom 
a small  triangular  tubercle,  giving  the  glabella  the  appearance  of  having  a 
projecting  angular  process  in  the  middle  of  its  front.”  I am  more  inclined  to 
view  this  triangular  tubercle  as  a point  of  attachment  for  the  muscles  of  the 
jaws,  and  not  as  a process  for  the  attachment  of  antennae. 

Mr.  E.  Billings  in  the  same  book  gives  a description  of  a second  species, 
which  he  calls  Shumardia  glacialis,  figured  p.  283,  tig.  270.  The  species  is 
represented  with  three  glabella  furrows,  and  should  not  be  included  in  the 
genus  Shumardia. 

If  these  forms  are  not  embryonic,  against  which  in  the  case  of  Conophrys 
salopiensis  Mr.  C.  Callaway  dissents  on  account  of  the  constant  size  of  the 
heads  and  the  absence  of  the  facial  sutures  amongst  the  larger  specimens,  I 
would  advocate  the  acceptance  of  the  new  genus  Shumardia  amongst  the  Agnos- 
tidce for  such  species  as  Shumardia  granulosa  and  Battus  pusillus  to  rejilace  the 
latter  generic  term  of  Conophrys. 

Bull.  63 10 


146 


A BIBLIOGRAPHY  OF  PALEOZOIC  CRUSTACEA. 


[BULL.  63. 


Solenopleura  Angelin,  1854;  Palseont.  Scand.,  p.  26. 

Type,  Solenopleura  holometopa  Angelin. 

Diagnosis:  Glabella  prominent,  with  three  distinct  furrows;  fixed  cheeks, 
elevated  especially  in  the  middle;  front  limb  convex;  occipital  ring  bearing  a 
tubercle;  genal  angles  pointed;  thorax,  pleurae  bluntly  rounded;  pygidium 
small  with  few  segments;  surface  of  shell  granulated  with  or  without  scat- 
tered tubercles. 

acadia  Whiteaves,  1885 ; Trans.  Royal  Soc.  Canada,  vol.  3,  p.  76,  pi.  7,  fig.  15. 

Cambrian. 

acadia  Whiteaves,  1887 ; Trans.  Royal  Soc.  Canada,  vol.  4,  p.  157,  pi.  2,  figs. 

5 a,  b,  c. 

acadia  var.  elongata  Matthew,  1887  ; idem,.,  p.  159,  pi.  1,  fig.  6. 

bombifrons  Matthew,  1886 ; Trans.  Royal  Soc.  Canada,  vol.  2,  p.  156,  figs.  5-5  a b. 

St.  John. 

communis  Billings,  1874  ; Pal.  Foss.,  vol.  2,  p.  72.  Potsdam. 

communis  Matthew,  1886 ; Trans.  Royal  Soc.  Canada,  vol.  2,  p.  155,  figs.  4-4  a,  b. 

nana  Ford,  1878;  Am.  Jour.  Sci.,  3d  series,  vol.  15,  p.  126.  Potsdam. 

nana  Walcott,  1886;  Bull.  U.  S.  Geol.  Survey,  No.  30,  p.  214,  pi.  27,  fig.  3. 

? nana  Walcott,  1887 ; Am.  Jour.  Sci.,  3d  series,  vol.  34,  p.  196,  pi.  1,  figs.  1-1  d. 

Cambrian. 

orestes  (Hartt)  Matthew,  1887 ; Trans.  Royal  Soc.  Canada,  vol.  4,  p.  154,  pi.  2, 

figs.  4 a-e. 

Syn.,  robbi  (Hartt)  Matthew,  1887;  Trans.  Royal  Soc.  Canada,  vol.  4,  p.  153, 
pi.  2,  figs.  3 a-1  and  figs.  4 a-e.  St.  John. 

? tumida  Wak^ptt,  1887 ; Am.  Jour.  Sci.,  3d  series,  vol.  34,  p.  196,  pi.  1,  fig.  2, 2 a. 

Cambrian. 

Sphaerexochus  Beyrich,  1845  ; Ueber  einige  bohmische  Trilobiten,  p.  19. 

Type,  Sphcerexochus  minis. 

canadensis  Billings,  1866  ; Catalogue  Sil.  Foss.  Anticosti,  p.  64,  fig.  21. 

mirus  (Beyrich) Roemer,  1860 ; Die  Sil.  Fauna  W.  Tennessee,  p.  81,  pi.  5,  fig.  20. 

Niagara. 

parvus  Billings,  1865;  Pal.  Foss.,  vol.  1,  p.  180,  fig.  161.  Chazy  and  Trenton. 

romingeri  Hall,  1862;  Geol.  Rept.  Wisconsin,  p.  434.  Niagara. 

Syn.,  mirus  Hall  (not  Beyrich),  1867 ; 20th  Rept.  New  York  State  Cab.  Nat. 
Hist.,  p.  334,  pi.  21,  figs.  4-7. 

romingeri  Hall,  1867 ; 20th  Rept.  New  York  State  Cab.  Nat.  Hist.,  p.  375,  pi.  22, 

figs.  4-7. 

romingeri  Hall,  1870;  20th  Rept.  New  York  State  Cab.  Nat.  Hist.,  p.  425,  pi. 

21,  figs.  4-7  (rev.  ed.). 

romingeri  Whitfield,  1882;  Geol.  Wisconsin,  vol.  4,  p.  311,  pi.  21,  figs.  1-3. 

romingeri  ? Hall;  28th  Rept.  New  York  State  Mus.  Nat.  Hist.,  p.  32,  pi.  32,  fig.  16. 

romingeri  Meek  and  Worthen,  1875;  Geol.  Survey  Illinois,  vol.  6,  p.  510,  pi.  24, 

fig.  4. 

Sphaerocoryphe  Angelin,  1854 ; Palaeont.  Scand.,  p.  65. 

Type,  Sphcerocori/phe  dentata  Angelin. 

robustus  Walcott,  1875;  Cincinnati  Quart.  Jour.  Sci.,  vol.  2,  p.  273,  figs.  18  a,  b. 

Trenton. 

salteri  Billings,  1866 ; Catalogue  Sil.  Foss.  Anticosti,  p.  63. 

Symphysurus  Goldfuss,  1843;  Jahrb.  fiir  Mineral.,  1843,  p.  552. 

— - ? goldfussi  Walcott,  1884;  Pal.  Eureka  Dist.,  Mon.  U.  S.  Geol.  Survey,  vol.  8, 
p.  95,  pi.  12,  fig.  16.  Pogonip. 

Telephus  Barrauae,  1852;  Syst.  Sil.  Boheme,  vol.  1,  p.  890. 

americanus  Billings,  1665;  Pal.  Foss.,  vol.  1,  p 291,  figs.  281.  Quebec. 

Terataspis  Hall,  1863;  16th  Rept.  New  York  State  Cab.  Nat.  Hist.,  p.  223.  (See 
Lichas  and  Acidaspis.) 

grandis.  (See  Lichas  [ Terataspis ] grandis  Hall.) 


VOGDES.] 


CATALOGUE  OF  TRILOBITES. 


147 


Terataspis  eriops.  (See  Lichas  [ Conolichas ] eriops  Hall.) 

Thaleops  Conrad,  1843;  Proc.  Acad.  Nat.  Sci.  Phila.,  vol.  1,  p.  332. 

ovatus  Conrad.  (See  Illaenus  ovatus. ) 

Triarthrella  Hall,  1863;  16th  Rept.  New  York  State  Cab.  Nat.  Hist.,  p.  177. 

auroralis  Hall,  1863  ; 16th  Rept.  New  York  State  Cab.  Nat.  Hist.,  p.  177,  pi.  9, 

fig.  13.  Potsdam. 

Triarthrus  Green,  1832 ; Monthly  Am.  Jour.  Geol.,  vol.  1,  p.560  (June).  Green,  1832; 
Mon.  Tril.  North  America,  p.  86. 

Type,  Triarthrus  beckii  Green. 

beckii  Green,  1832;  Monthly  Am.  Jour.  Geol.,  vol.  1,  p.  560,  pi.  1,  fig.  3 (June). 

beckii  Green,  1832;  Mon.  Tril.  N.  A.,  p.  86,  cast  34,  pi.  1,  fig.  3. 

beckii  Harlan,  1835;  Trans.  Geol.  Soc.  Penn.,  vol.  1,  p.  205,  pi.  15,  fig.  6. 

Syn.,  [ Parqdoxides]  triarthrus  Harlan,  1835;  Trans.  Geol.  Soc.  Penn.,  vol.  1,  pi. 
p.  264,  15,  fig.  5. 

[Paradoxides']  arcuatus  Harlan,  1835;  Trans.  Geol.  Soc.  Penn.,  vol.  1,  p. 
265,  pi.  15,  figs.  1-3. 

beckii  Harlan,  1835;  Med.  Phys.  Researches,  p.  400,  pi.,  fig.  6. 

Syn.,  [ Paradoxides}  triarthrus  Harlan,  1835;  Med.  Phys.  Researches,  p.  401,  pi., 
fig.  5. 

[ Paradoxides ] arcuatus  Harlan,  1835;  Med.  Phys.  Researches,  p.  402,  pi., 
figs.  1-3. 

beckii  Green,  1835  ; Suppl.  Mon.  Tril.  N.  A.,  p.  vii. 

[ Paradoxides ] beckii  Hall,  1838;  Am.  Jour.  Sci.,  1st  series,  vol.  33,  p.  142,  fig.  2. 

Syn.,  Paradoxides  eatoni  Hall,  1838;  Am.  Jour.  Sci.,  1st  series,  vol.  33,  p.  142, 
fig.  2. 

beckii  Green,  1838 ; Am.  Jour.  Sci.,  1st  series,  vol.  33,  p.  344. 

beckii  Mather,  1842;  Geol.  New  York,  1st  Geol.  Dist.,  p.  390,  fig.  24  (1). 

beckii  Emmons,  1842;  Geol.  New  York,  2d  Geol.  Dist.,  p.  399,  fig.  110  (1). 

beckii  Yanuxem,  1843;  Geol.  New  York.,  3d  Geol.  Dist.,  p.  57,  fig.  8 (1). 

beckii  Hall.  1843;  Geol.  New  York,  4th  Geol.  Dist.,  p.  504. 

[ Calymene ] beckii  Hall,  1847;  Pal.  New  York,  vol.  1,  p.  237,  pi.  64,  figs.  2 a-e. 

[ Calymene ] beckii  Hall,  1847;  Pal.  New  York,  vol.  1,  p.  250,  pi.  66,  figs.  2 a-k 

(not  pi.  67,  figs.  4 a-e,  Atops  triliueatus). 

Syn.,  Atops  triliueatus  (Emmons)  Hall,  1847;  Pal.  New  York,  vol.  1,  p.  237. 

[ Calymene ] becki  Hall,  1848 ; Am.  Jour.  Sci.,  2d  series,  vol.  5,  p.  322,  figs.  1 a,  b, 

2 a-g. 

becki  Emmons,  1848 ; Am.  Assoc.  Adv.  Sci.,  p.  17. 

beckii  Haldeman,  1848;  Am.  Jour.  Sci.,  2d  series,  vol.  8,  p.  137. 

beckii  Emmons,  1855;  Am.  Geology,  vol.  1,  pt,  2,  p.  214,  pi.  15,  fig.  12. 

[ Calymene ] beckii  Rogers,  1858;  Geol.  Survey  Penn.,  vol.  2,  p.  820,  fig.  613. 

beckii  Barraude,  1861 ; Soc.  Gdol.  France,  2d  series,  p.  269,  pi.  5,  figs.  11, 12. 

beckii  Logan,  1863;  Geol.  Canada,  p.  202,  fig.  200. 

beckii  Miller,  1874;  Cincinnati  Quart.  Jour.  Sci.,  vol.  1,  p.  146. 

becki  Walcott,  1876;  Trans.  Albany  Inst.,  vol.  10,  p.  23,  pi.  2,  figs.  1-16. 

Trenton. 

[Brongniartia]  carcinodea  Eaton,  1832;  Am.  Jour.  Sci.,  1st  series,  vol.  22,  p. 

166  (March  6). 

[ Brongniartia ] carcinodea  Eaton,  1832;  Geol.  Text  Book,  p.  33,  pi.  1,  fig.  3. 

canadensis  Smith,  1861 ; Canadian  Jour.,  vol.  6,  p.  275.  Hudson. 

fischeri  Billings,  1861;  Pal.  Foss.,  vol.  1,  p.  291,  fig.  280.  Quebec. 

glaber  Billings,  1859;  Canadian  Naturalist,  vol.  4,  p.  382.  Utica. 

glaber  Billings,  1863;  Geol.  Canada,  p.  202,  fig.  198. 

spinosus  Billings,  1859;  Canadian  Naturalist,  vol.  4,  p.  382.  Trenton. 

spinosus  Billings,  1863;  Geol.  Canada,  p.  202,  fig.  199. 

spinosus  Ami,  1882;  Trans.  Ottawa  Nat.  Club,  vol.  for  1882-’83,  p.  88,  pi.  1,  figure. 


148  A BIBLIOGRAPHY  OF  PALEOZOIC  CRUSTACEA.  [bull.  63. 

Triarthrus  trimerus  Green,  1832;  Monthly  Am.  Jour.  Geol.,  vol.  1,  p.  560.  (See  Ho- 
malonotus  delphinocephalus  and  H.  jacksoni.) 

Trinucleus  Lhwyd,  1698;  Lithophyacii  Britannici  Ichnograpliia,  Epistola  1.  Mur- 
chison, Silurian  System,  1839,  p.  659. 

Sir  R.  I.  Murchison  has  revived  this  old  name  of  Lhwyd’s  from  classical  feel- 
ings, and  all  subsequent  palaeontologists  have  adopted  it.  Lhwyd’s  description 
meant  no  more  than  the  general  name  of  Trilobite  of  the  more  modern  writers, 
and  could  not,  except  by  courtesy,  set  aside  Dr.  Jacob  Green’s  genus  Cryptolithus. 

bellulus  Ulrich,  1878 ; Jour.  Cincinnati  Soc.  Nat.  Hist.,  vol.  1,  p.  99,  pi.  4,  fig.  15. 

INuttainia ] concentrica  Eaton,  1832;  Geological  Text  Book,  p.  34,  pi.  1,  fig.  2. 

Syn.,  Trilobite  Bigsby,  1825;  Annals  Lyceum  Nat.  Hist.  New  York,  vol.  1,  pt.  2, 
p.  214,  pi.  15,  fig.  1.  Trenton  and  Hudson. 

Cryptolithus  tessellatus  Green,  1832;  Mon.  Tril.  N.  A.,  p.  73,  cast  38,  pi.  1,  fig.  4. 

Cryptolithus  tessellatus  Green,  1832;  Monthly  Am.  Jour.  Geol.,  vol.  1,  pi.  1, 
fig.  4. 

concentrica  Hall,  1847  ; Pal.  New  York,  vol.  1,  pp.  249, 255,  pi.  65,  figs.  4 a,  b ; pi. 

67,  figs.  1 a-h. 

concentrica  Emmons,  1855 ; Am.  Geology,  vol.  1,  pt.  2,  p.  212,  pi.  17,  fig.  1. 

concentrica  Chapman,  1858;  Canadian  Jour.,  vol.  3,  p.  514. 

concentrica  Billings,  1861 ; Geol.  Vermont,  vol.  1,  p.  300,  fig.  215. 

concentrica  Miller,  1874 ; Cincinnati  Quart.  Jour.  Sci.,  vol.  1,  p.  126. 

Zacanthoides  Walcott,  1887  ; Am.  Jour.  Sci.,  3d  series,  vol.  36,  p.  165. 

Type,  Zacanthoides  spinosus  Walcott. 

[Dicellocephalus?  j flagricauda  White,  1874;  Prelim.  Rept.  Invt.  Foss.  Geog.  aud 

Geol.  Survey  ^Vest  100th  Mer.,  p.  12.  Cambriau. 

[ Dicellocephalus  ? ] flagricauda  White,  1877  ; U.  S.  Geog.  and  Geol.  Survey  West 

100th  Mer.,  vol.  4,  p.  60,  pi.  3,  figs.  8 a,  b. 

[ Olenoides ] flagricauda  Walcott,  1886 ; Bull.  U.  S.  Geol.  Survey,  No.  30,  p.  185,  pi. 

25,  fig.  4. 

flagricauda  Walcott,  1888 ; Am.  Jour.  Sci.,  3d  series,  vol.  36,  p.  165. 

[Olenoides ] levis  Walcott,  1886 ; Bull.  U.  S.  Geol.  Survey,  No.  30,  p.  187,  pi.  25,  figs. 

3,3  a.  CambriaD. 

levis  Walcott,  188'8;  Am.  Jour.  Sci.,  3d  series,  vol.  36,  p.  165. 

[.Ogygiaf]  spinosus  Walcott,  1884  ; Pal.  Eureka  Dist.,  Mon.  U.  S.  Geol.  Survey, 

vol.  8,  p.  63,  pi.  9,  fig.  22.  Middle  Cambrian. 

[ Olenoides ] spinosus  Walcott,  1886 ; Bull.  U.  S.  Geol.  Survey,  No.  30,  p.  184,  pi.  25, 

figs,  6, 6 a. 

[Embolimus~\  spinosus  (Rominger)  Walcott,  1888;  Am.  Jour.  Sci.,  3d  series,  vol. 

36,  p.  164. 

spinosus  Walcott,  1888 ; Am.  Jour.  Sci.,  3d  series,  vol.  36,  p.  165. 

[ Olenoides ] typicalis  Walcott,  1886 ; Bull.  U.  S.  Geol.  Survey,  No.  30,  p.  183,  pi.  25, 

figs.  2, 2 a.  Middle  Cambrian. 

typicalis  Walcott,  1888 ; Am.  Jour.  Sci.,  3d  series,  vol.  36,  p.  165. 


PART  III. 


CATALOGUE  OF  NON-TRILOBITES. 

mk  ■ - - - - - - ■ - — - ■ - 


149 


PART  III 


NON-TRILOBITIC  GENERA  AND  SPECIES. 


MEROSTOMATA. 

EURYPTERIDiE. 

Eurypterus  De  Kay,  1825;  Annals  Lyceum  Nat.  Hist.,  vol.  1,  p.  375. 
Dolichopterus  Hall,  1859;  Palaeont.  New  York,  vol.  3,  p.  414. 

Echinognathus  Walcott,  1882;  Am.  Jour.  Sci.r  3d  series,  vol.  23,  p.  213. 
Adelophthalmus  Jordan  and  Meyer,  1854;  Crust.  Steinkohl.  Saarb.,  p.  8. 
Glyptoscorpius  Peach,  1880;  Trans.  Royal  Soc.  Edinb.,  vol.  30,  p.  516. 
Arthropleura  Jordan  and  Meyer,  1854  ; Crust.  Steinkohl.  Saarb.,  p.  13. 

PTERYGOTIDiE. 

Pterygotus  Agassiz,  1844;  Mon.  Poissons  Foss.,  note,  p.  xix. 

Slimonia  Page,  1856 ; Advance  Text-Book  Geology,  p.  135. 

Stylonurus  Page,  1856 ; Advance  Text-Book  Geology. 

SYNZIPHOSURA. 

Acanthotelson  Meek  and  Worthen,  1865 ; Proc.  Acad.  Nat.  Sci.  Phila.,  vol.  17,  p.  46 
Geol.  Survey  Illinois,  vol.  2,  1866,  p.  399. 

4 

XIPHOSURA. 

CYCLID.®. 

Cyclus  De  Koninck,  1841 ; M6m.  Acad.  Sci.  Belgique,  vol.  14,  p.  13. 

Dipeltis  Packard,  1885;  American  Naturalist,  vol.  19,  p.  293. 

BUNODIDvE. 

Bunodes  Eichwald,  1854 ; Beitriige  Geol.  u.  Pal.  Russ.,  p.  131. 

Hemisapis  Woodward,  1865;  Quart.  Jour.  Geol.  Soc.  London,  vol.  21,  p.  490. 
Exapinurus  Nieszkowski,  1859;  Archiv  Nat.  Liv-,  Esth-  u.  Kurl.,  vol.  1,  p.  380. 
Pseudoniscus  Neiszkowski,  1859;  Archiv  Nat.  Liv-,  Esth-  u.  Kurl.,  vol.  1,  p.  381. 

LIMULID^E. 

Belinurus  Koenig,  1820 ; leones  Foss.  Sec  tiles,  pi.  18,  fig.  230. 

Prestwichia  Woodward,  1887 ; Quart.  Jour.  Geol.  Soc.  London,  vol.  23,  p.  32. 

151 


152 


A BIBLIOGRAPHY  OF  PALEOZOIC  CRUSTACEA. 


[BULL.  63. 


Limulus  Muller,  1785;  Entomostraca,  etc.,p.  124. 

Protolimulus  Packard,  1886;  Mem.  Nat.  Acad.  Sci.,  vol.  3,  p.  150. 

Neolimulus  Woodward,  1868;  Geol.  Mag.,  vol.  5,  p.  1. 

PHYLLOPODA. 

CERATIOCARIDiE. 

Hymenocaris  Salter,  1852;  Rept.  22d  Meeting  Brit.  Assoc.  Adv.  Sci.,  Trans.  Sec., 
p.  56. 

Ceratiocaris  McCoy,  1849 ; Annals  Mag.  Nat.  Hist.  London,  2d  series,  vol.  4,  p.  412. 
Echinocaris  Whitfield,  1880;  Am.  Jour.  Sci.,  3d  series,  vol.  19,  p.  34. 

Didyocaris  Salter,  1860 ; Annals  Mag.  Nat.  Hist.  London,  3d  series,  vol.  5,  p.  161. 
Dithyocaris  (Scouler)  Portlock ; Geol.  Rept.  Londonderry,  etc.,  1843,  p.  313. 
Protocaris  Walcott,  1884;  Bull.  U.  S.  Geol.  Survey,  No.  10,  p.  50. 

Elymocaris  Beecher,  1884  ; 2d  Geol.  Survey  Penn.,  vol.  PPP.,  p.  13. 

Tropidocaris  Beecher,  1884;  2d  Geol.  Rept.  Penn.,  vol.  PPP.,  p.  15. 

Physocaris  Salter,  1860 ; Annals  Mag.  Nat.  Hist.  London,  3d  series,  vol.  5,  p.  159. 
Phasganocaris  Novak,  1886  ; Sitzungsb.  bohm.  Gesell.,  1886,  p.  498. 

Acanthocaris  Peach,  1882;  Trans.  Royal  Soc.  Edinb.,  vol.  30,  p.  511. 

DISCINOCARHLE. 

Discinocaris  Woodward,  1866;  Quart.  Jour.  Geol.  Soc.  London,  vol.  22,  p.  504. 
Spathiocaris  Clarke,  1882;  Am.  Jour.  Sci.,  3d  series,  vol.  23,  p.  477. 

Pholadocaris  Woodward,  1882;  Geol.  Mag.,  decade  3,  vol.  9,  p.  388. 

Ellipsocaris  Woodward,  1882 ; Geol.  Mag.,  decade  3,  vol.  9,  p.  444. 

Lisgocaris  Clarke,  1882;  Am.  Jour.  Sci.,  3d  series,  vol.  23,  p.  478. 

Cardiocaris  Woodward,  1882  ; Geol.  Mag.,  decade  3,  vol.  9,  p.  386. 

Dipterocaris  Clarke,  1883 ; Am.  Jour.  Sci.,  3d  series,  vol.  23,  p.  121. 

Pterocaris  Barrande,  1872  ; Syst.  Sil.  Boheme,  vol.  1,  suppl.,  p.  464. 

Crescentella  Barrande,  1872;  Syst.  Sil.  Boheme,  vol.  1,  suppl.,  p.  507. 
Aptychopsis  Barrande,  1872 ; Syst.  Sil.  Boheme,  vol.  1,  suppl.,  p.  455. 

Peltocaris  Salter,  1863 ; Quart.  Jour.  Geol.  Soc.  London,  vol.  19,  p.  87. 

Pinnocaris  Etheridge,  1878;  Proc.  Royal  Phys.  Soc.,  Edinb.,  vol.  4,  p.  167. 
Ptychocaris  Novak,  1885;  Sitzungsb.  bohm.  Gesell.,  1885,  p.  343. 

RHINOCARHLE. 

Rhinocaris  Clarke,  1888  ; Palaeont.  New  York,  vol.  7,  p.  lviii. 

Colpocaris  Meek,  1871;  Proc.  Acad.  Nat.  Sci.  Phila.,  vol.  23,  p.  334. 

Solenocaris  Meek,  1871 ; Proc.  Acad.  Nat.  Sci.  Phila.,  vol.  23,  p.  335.  Name  should 
be  changed,  preoccupied  by  J.  Young.  See  Strigocaris. 

Mesothyra  Hall,  1888 ; Palaeont.  New  York,  vol.  7,  pp.  lvi,  187. 

Sacocaris  Salter,  1868;  Proc.  Geol.  Poly  tech.  Soc.,  vol.  4,  p.  588. 

Lingulocaris  Salter,  1866 ; Mem.  Geol.  Survey,  vol.  3,  pp.  252, 253,  and  294. 
Solenocaris  Young,  1868  ; Proc.  Nat.  Hist.  Soc.  Glasgow,  vol.  1,  p.  171. 

Rostrocaris  Kinnear,  1887;  Trans.  Edinb.  Geol.  Soc.,  vol.  5,  p.  417. 

Caryocaris  Salter,  1863;  Quart.  Jour.  Geol.  Soc.  London,  vol.  19,  p.  139. 
Entomidella  Jones,  1873  ; Annals  Mag.  Nat.  Hist.,  London,  4th  series,  vol.  11,  p:  416. 
Arch^cocaris  Meek,  1872  ; Proc.  Acad.  Nat.  Sci.  Phila.,  vol.  23,  p.  335. 

Myocaris  Salter,  1864 ; Quart.  Jour.  Geol.  Soc.  London,  vol.  20, 1864,  p.  292. 
Estheria  Ruppell,  1857  ; Mus.  Senckenberg,  vol.  2,  p.  119. 

Leaia  Jones,  1882 ; Mon.  Fossil  Estheria,  p.  115. 

Schizodiscus  Clarke,  1888;  Palaeont.  New  York,  vol.  7,  p.  207. 


VOGDES.  ] 


CATALOGUE  OF  NON-TRILOBITES. 


153 


BIVALVED  ENTOMOSTRACA. 

CYPRIDINID^E. 

Cypridina  Milne-Ed wards,  1838;  Lamarck’s  Anim.  s.  Vert.,  vol.  5,  p.  178. 
Cypridinella  Jones  and  Kirkby,  1874;  Mon.  Carboniferous  Eutom.,  p.  21. 
Cypridellina  Jones  and  Kirkby,  1874;  Mon.  Carboniferous  Entom.,  p.  25. 

Sulcuna  Jones,  1873;  Quart.  Jour.  Geol.  Soc.  London,  vol.  29.  p.  411. 

, Cyprella  De  Koninck,  1841 ; M6m.  Acad.  Royale  Bruxelles,  vol.  14,  p.  19. 
Bradycinetus  Sars,  1865  ; Oversigt  af  Norges  Marine  Ostracoder. 

Philomedes  Lilljeborg,  1853 ; Crust,  in  Scania  Occurrentibus,  p.  175. 

Rhombina  Jones  and  Kirkby,  1874  ; Mon.  Carboniferous  Entom.,  p.  43. 

ENTOMOCONCHIDiE. 

Entomoconchus  McCoy,  1839;  Jour.  Geol.  Soc.  Dublin,  vol.  2,  p.  91. 

Offa  Jones  and  Kirkby,  1874;  Mon.  Carboniferous  Entom.,  p.  53. 

POLYCOPID.E. 

Polycope  Sars,  1865 ; Oversigt  af  Norges  Marine  Ostracoder. 

ENTOMIDID^E. 

Entomis  Jones,  1861 ; Mem.  Geol.  Survey  Scotland,  Expl.  map  32,  p.  137. 

CYTHERELLHLE. 

Cytherella  Jones  and  Bosquet,  1848  and  1852. 

Cytherellina  Jones  and  Holl,  1869;  Annals  Mag.  Nat.  Hist.,  London,  4th  series, 
vol.  3,  p.  215. 

Cytherina  Lamarck,  1818;  Animaux  sans  Vert.,  vol.  5,  p.  125. 

JEchmixa  Jones  and  Holl,  1869 ; Annals  Mag.  Nat.  Hist.,  London,  4th  series,  vol.  3, 
p.  217. 

LEPERDITIDiE. 

Leperditia  Rouault,  1851 ; Bull.  Soc.  G6ol.  France,  2d  series,  vol.  8,  p.  377. 

Bernix  Jones,  1884  ; Proc.  Berwickshire  Nat.  Club,  vol.  10,  p.  316. 

Isochilin a Jones,  1858;  Annals  Mag.  Nat.  Hist.,  London,  3d  series,  vol.  1,  p.  248. 
Primitia  Jones  and  Holl,  1865 ; Annals  Mag.  Nat.  Hist.,  Loudon,  3d  series,  vol.  16, 
p.  416. 

Beyrichia  McCoy,  1846 ; Synopsis  Sil.  Foss.  Ireland,  p.  57. 

Beyrichiella  Jones  and  Kirkby,  1886  ; Geol.  Mag.,  n.  s.,  decade  3,  vol.  3,  p.  438. 
Kirkbya  Jones,  1869;  Annals  Mag.  Nat.  Hist.,  London,  4th  series,  vol.  3,  p.  223. 

Moo rea  Jones  and  Kirkby,  1867  ; Annals  Mag.  Nat.  Hist.,  London,  4th  series,  vol.  3, 
p.  225. 

Phreatura  Jones  and  Kirkby,  1886;  Quart.  Jour.  Geol.  Soc.  London,  vol.  42,  p.  507. 

I Strepula  Jones  and  Holl,  1886  ; Annals  Mag.  Nat.  Hist.,  London,  5th  series,  vol.  17, 

p.  403. 

| Bollia  Jones  and  Holl,  1886 ; Annals.  Mag.  Nat.  Hist.,  London,  5th  series,  vol.  17, 
[ p.  360. 

B Kl(EDINIA  Jones  and  Holl,  1886  ; Anuals  Mag.  Nat.  Hist.,  London,  5th  series,  vol.  17, 
p.  362. 

ri  Beyrichiopsi8  Jones  and  Kirkby,  1886  ; Geol.  Mag.,  decade  3,  vol.  3,  p.  434. 

II  Aparchites  Jones,  1889;  Annals  Mag.  Nat.  Hist.,  6th  series,  vol.  3,  p.  385. 
Primitopsis  Jones,  1887;  Notes  on  some  Sil.  Ostracoda  from  Gothland,  p.  5. 

; 


154  A BIBLIOGRAPHY  OF  PALEOZOIC  CRUSTACEA.  [bull.  63. 

Placentura  Jones  and  Holl,  1886;  Annals  Mag.  Nat.  Hist.,  London,  5th  series,  vol. 
17,  p.  407. 

Kyamodes  Jones,  1888;  Annals  Mag.  Nat.  Hist.,  London,  6th  series,  vol.  2,  p.  295. 
Cyprosis  Jones,  1881 ; Geol.  Mag.,  decade  2,  vol.  8,  p.  338. 

Cyprosina  Jones,  1881 ; Geol.  Mag.,  decade  2,  vol.  8,  p.  338. 

Octonaria  Jones,  1887;  Annals  Mag.  Nat.  Hist.,  London,  5th  series,  vol.  19,  p.  404. 

CYPRIDJE. 

Aglaia  Brady,  1867;  Challenger  Exped.,Rept.  on  Ostracoda,  p.  33. 

Candona  Baird,  1850 ; History  Brit.  Entomostraca,  p.  159. 

ARGILL.ECIA  Sars,  1865 ; Ofversigt  af  Norges  Marine  Ostracoder. 

Macrocypsis  Brady,  1867 ; Intellectual  Observ.,  vol.  12,  p.  119. 

Bathocypsis  Brady,  1880;  Challenger  Exped.,  Rept.  on  Ostracoda,  p.  45. 

Bairdia  McCoy,  1844 ; Synopsis  Carboniferous  Foss.  Ireland,  p.  164. 

DARWINULIDiE. 

Darwinula  (Brady  and  Robertson)  Jones,  1885;  Quart.  Jour.  Geol.  Soc.,  vol.  41,  p. 
346.  Name  changed  from  preoccupied  term  Darwinella  (Ann.  Mag.  Nat.  Hist., 
4th  series,  vol.  9,  1872,  p.  50). 

CYTHERIDiE. 

CYTHERE  Muller,  1785 ; Entomostraca,  etc.,  p.  64. 

Xestoleberis  Sars,  1865 ; Ofversigt  af  Norges  Marine  Ostracoder,  p.  68. 
Bythocythere  Sars,  1865;  Ofversigt  af  Norges  Marine  Ostracoder. 

Carbonia  Jones,  1870;  Geol.  Mag.,  vol.  7,  p.  218. 

Youngia  Jones  and  Kirkby,  1886;  Quart.  Jour.  Geol.  Soc.  London,  vol.  42,  p.  507. 
Thlipeura  Jones  and  Holl,  1869 ; Annals  Mag.  Nat.  Hist.,  London,  4th  series,  vol.  3, 
p.  213. 

Bursulella  Jones,  1887 ; Notes  on  some  Sil.  Ostracoda  from  Gothland,  p.  7. 
Aristozoe  Barrande,  1872;  Syst.  Sil.  Boheme,  vol.  1,  suppl.,  p.  474. 

Orozoe  Barrande,  1872;  Syst.  Sil.  Boheme,  vol.  1,  suppl.,  p.  537. 

Callizoe  Barraude,  1872;  Syst.  Sil.  Boheme,  vol.  1,  suppl.,  p.  503. 

Zonozoe  Barrande,  1872 ; Syst.  Sil.  Boheme,  vol.  1,  suppl.,  p.  554. 

Hippa  Barrande,  1872;  Syst.  Sil.  Boheme,  vol.  1,  suppl.,  p.  516. 

Bolbozoe  Barrande,  1872;  Syst.  Sil.  Boheme,  vol.  1,  suppl.,  p.  500. 

Elpe  Barrande,  1872;  Syst.  Sil.  Boheme,  vol.  1,  suppl.,  p.  510. 

Nothozoe  Barrande,  1872 ; Syst.  Sil.  Boheme,  vol.  1,  suppl.,  p.  536. 

Caryon  Barrande,  1872;  Syst.  Sil.  Boheme,  vol.  1,  suppl., p.  505. 

Cryptozoe  Packard,  1888;  Proc.  Acad.  Nat.  Sci.  Phila.,  1888,  p.  381. 

Cytheropsis  (McCoy)  Barrande,  1872;  Syst.  Sil.  Boheme,  vol.  1,  suppl.,  p.  508. 

CIRRIPEDJE. 

Plumulites  Barrande,  1872;  Syst.  Sil.  Boheme,  vol.  1,  suppl.,  p.  565. 

Strobilepis  Clarke,  1888;  Palseont.  New  York,  vol.  7,  p.  212. 

Paleocreusia  Clarke,  1888 ; Palseont.  New  York,  vol.  7,  p.  210. 

Protobalanus  Whitfield,  1888;  Palseont.  New  York,  vol.  7,  p.  lxii;  Bull.  Am.  Mus. 
Nat.  Hist.,  vol.  2,  1889,  p.  66. 

Turrilepas  Woodward,  1865;  Quart.  Jour.  Geol.  Soc.  London,  vol.  21,  p.  489. 

DECAPODA. 

Anthrapalemon  Salter,  1861 ; Quart.  Jour.  Geol.  Soc.  London,  vol.  17,  p.  529. 
Paleopalemon  Whitfield,  1880;  Am.  Jour.  Sci.,  3d  series,  vol.  19,  p.  40. 
Crangopsis  Salter,  1863;  Quart.  Jour.  Geol.  Soc.  London,  vol.  19,  p.  80. 
Pseudo-Galathea  Peach,  1882;  Trans.  Royal  Soc.  Edinb.,  vol.  30,  p.  573. 


VOGDEB.] 


CATALOGUE  OF  NON-TR1LOBITES. 


155 


SCHIZOPODA. 

Gampsonyx  Meyer,  1847  ; Verhandl.  Nat.  Vereins  Preuss.,  vol.  4,  p.  86. 
Pal^eocaris  Meek  and  Worthen,  1865 ; Proc.  Acad.  Nat.  Sci.  Phila.,  p.  48. 
Nkctotelson  Brocchi,  1880 ; Bull.  Soc.  G6ol.  France,  3d  series,  vol.  8,  p.  10. 

AMPHIPODA. 

Diplostylus  Salter,  1863 ; Quart.  Jour.  Geol.  Soc.  London,  vol.  19,  p.  76. 

STEOMAPODA. 

Amphipeltis  Salter,  1863 ; Quart.  Jour.  Geol.  Soc.  London,  vol.  19,  p.  75. 


CATALOGUE  OF  NORTH  AMERICAN  PALEOZOIC  CRUSTACEA— NON- 

TRILOBITA. 


(Current  generic  names  in  bold  face ; synonyms  in  Italic .] 

Acanthotelson  Meek  and  Worfchen,  1865 ; Proc.  Acad.  Nat.  Sci.  Phila.,  vol.  17,  p.  46  • 
Geol.  Survey  Illinois,  vol.  2, 1866,  p.  299. 

Type,  A.  stimsoni. 

eveni  Meek  and  Worfchen,  1868 ; Am.  Jour.  Sci.,  2d  series,  vol.  46,  p.  28. 

. „ Coal  Measures, 

eveni  Meek  and  Worthen,  1868  ; Geol.  Survey  Illinois,  vol.  3,  p.  551,  figs.  a-d. 

! eveni  White,  1884  ; 13th  Rept.  Dept.  Geol.  Nat.  Hist.  Indiana,  p.  177,  pi.  38,  figs. 

I eveni  Packard,  1886;  Mem.  Nat.  Acad.  Sci.,  vol.  3,  p.  125. 

| inequalis.  (See  Falaeocaris  typus.) 

? magister  Packard,  1886 ; Mem.  Nat.  Acad.  Sci.,  vol.  3,  p.  127,  pi.  1 fig.  2 • pi. 

2,  figs.  4,  5.  Carboniferous, 

stimpsoni  Meek  and  Worthen,  1865;  Proc.  Acad.  Nat.  Sci.  Phila..  vol.  17,  p.  47. 

. . Coal  Measures, 

stimpsoni  Meek  and  Worthen,  1866 ; Geol.  Survey  Illinois,  vol.  2,  p.  401  pi  32 
figs.  6,  6 a-f.  ’ 

stimpsoni  Meek  and  Worthen,  1868 ; Geol.  Survey  Illinois,  vol.  3,  p.  549,  figs,  a,  b. 
stimpsoni  Woodward,  1881 ; Geol.  Mag.,  decade  2,  vol.  8,  p.  533,  pi.  14,  fig.  4. 
stimpsoni  White,  1884 ; 13th  Rept.  Dept.  Geol.  Nat.  Hist.  Indiana,  p.  176  pi.  37 
figs.  4,  5.  ’ ' ’ 

stimpsoni  Packard,  1886;  Mem.  Nat.  Acad.  Sci.,  vol.  3,  p.  124. 

Packard  considers  this  species  to  be  the  young  of  Acanthotelson  eveni. 
JEchmina  Jones  and  Holl,  1887;  Annals  Mag.  Nat.  Hist.,  5th  series,  vol.  3,  p.  217. 
byrnesi  (Miller)  Jones,  1890;  Quart.  Jour.  Geol.  Soc.,  vol.  46,  p.  12,  pi.  3,  figs. 

„ * , _ Cincinnati. 

b or  other  references,  see  Leperditia  byrnesi  Miller. 

spinosa  (Hall)  Jones,  1890;  Quart.  Jour.  Geol.  Soc.,  vol.  46,  p.  11,  pi.  3,  fig8. 

Niagara 

For  other  references,  see  Cytherina  spinosa  Hall. 

Amphipeltis  Salter,  1863  ; Quart.  Jour.  Geol.  Soc.  London,  vol.  19,  p.  75. 

paradoxus  Salter,  1863;  Quart.  Jour.  Geol.  Soc.  London,  vol.  19,  p.  76,  figs.  11 

’ , _ Devonian, 

paradoxus  Dawson,  1868;  Acadian  Geology,  p.  523,  fig.  180. 

* paradoxus  Salter  and  Woodward  ; Chart  of  Fossil  Crustacea,  pi.  3 fi«-  3 
Anthracovetes  Meek  and  Worthen,  1868;  Am.  Jour.  Sci.,  2d  eeriee,  vol.  46  p 21 

mazonensis  Meek  and  Worthen.  (See  Eurypterus  mazonensis  ) 

Anthrapaleemon  Salter,  1861;  Quart.  Jour.  Geol.  Soc.  London,  vol.  17  p.  52». 

Type,  A.  yrossarii  Salter.  ’ 

gracilis  Meek  and  Worthen,  1865 ; Proc.  Acad.  Nat.  Sci.  Phila.,  vol.  17,  p.  50. 

...  . Coal  Measures. 

gracilis  Meek  and  Worthen,  1866;  Geol.  Survey  Illinois,  vol.  2,  p.  407  pi  32 
figs.  4 a,  b,  c.  r ’ ’ 


157 


158 


A BIBLIOGRAPHY  OF  PALEOZOIC  CRUSTACEA. 


[BULL.  63. 


Anthrapaleemon  gracilis  Meek  and  Worthen,  1868;  Geol.  Survey  Illinois,  vol.  3,  p. 

554,  figs,  a,  b. 

gracilis  White,  1884 ; 13th  Rept.  Dept.  Geol.  Nat.  Hist.  Indiana,  p.  180,  pi.  38, 

figs.  8, 9. 

gracilis  Packard,  1885 ; American  Naturalist,  vol.  19,  p.  880. 

gracilis  Packard,  1886;  Mem.  Nat.  Acad.  Sci.,  vol.  3,  p.  135,  pi.  4,  figs.  1,2,  3, 5, 

6;  pi.  7,  figs.  3-6. 

[Palceocarabu8~\  hillianus  Dawson,  1878;  Geol.  Mag.,  vol.  4,  p.  56,  fig.  1. 

Coal  Measures. 

[ Palceocarabus ] hillianus  Dawson,  1878;  Suppl.  Acadian  Geology,  p.  55,  fig. 

10. 

Aparchites  Jones,  1889;  Annals  Mag.  Nat.  Hist.,  6th  series,  vol.  3,  p.  385. 

minutissimus  (Hall)  Ulrich,  1889;  Contributions  Micro-Palseont.,  pt.  2,  p.  49. 

For  other  references,  see  Leperditia  [ Isochilina ] minutissima  Hall.  Hudson. 

unicornis  Ulrich,  1889 ; Contributions  Micro-Palseont.,  pt.  2,  p.  50,  pi.  9,  fig.  11. 

For  other  references,  see  Leperditia  unicornis.  Hudson. 

Aptychopsis  Barrande,  1872;  Syst.  Sil.  Boheme,  vol.  1,  suppl.,  p.  436. 
Archaeocaris  Meek,  1871 ; Proc.  Acad.  Nat.  Sci.  Phila.,  vol.  23,  p.  335. 

vermiformis  Meek,  1871 ; Proc.  Acad.  Nat.  Sci.  Phila.,  vol.  23,  p.  335. 

Carboniferous. 

Aristozoe  Barrande,  1872 ; Syst.  Sil.  Boheme,  suppl.,  vol.  1,  p.  474. 

rotundata  Walcott,  1887 ; Am.  Jour.  Sci.,  3d  series,  vol.  34,  p.  193,  pi.  l,fig.  9. 

Cambrian. 

troyensis  (Ford)  Walcott,  1887 ; Am.  Jour.  Sci.,  3d  series,  vol.  34,  p.  193,  pi.  fig. 

8.  Cambrian. 

[ Leperditia ] troyensis  Ford,  1873 ; Am.  Jour.  Sci.,  3d  series,  vol.  6,  p.  138. 

Aristozoe  sp.  Shaler  and  Foerste,  1888;  Bull.  Mus.  Comp.  Zoology,  vol.  16,  p.  35,  pi. 

2,  fig.  18.  Cambrian. 

Belinurus  Koenig,  1820 ; leones.  Foss.  Sectiles,  p.  18,  fig.  230 ; Baily,  Annals  Mag.  Nat. 

Hist.,  London,  3d  series,  vol.  11, 1863. 

dance  Meek  and  Worthen.  (See  Frestwichia  danae.) 

laccei  Packard,  1885 ; American  Naturalist,  vol.  19,  p.  292.  Carboniferous. 

laccei  Packard,  1886;  Mem.  Nat.  Acad.  Sci.,  vol.  3,  p.  149,  pi.  5,  fig.  5. 

Beyrichia  McCoy,  1846;  Silurian  Foss.  Ireland,  p.  58. 

Type,  Beyrichia  Iclodeni  McCoy. 

eequilatera  Hall,  1860;  Canadian  Naturalist,  vol.  5,  p.  158,  fig.  20.  Silurian. 

aequilatera  Dawson,  1868;  Acadian  Geology,  p.  609,  fig.  217. 

aequilatera  Jones,  1890 ; Quart.  Jour.  Geol.  Soc.,  vol.  46,  p.  18,  pi.  2,  fig.  6. 

atlantica  Billings,  1865;  Pal.  Foss.,  vol.  1,  p.  300.  Quebec. 

bela  Walcott,  1883;  Description  New  Species  Trenton  Group,  p.  7,  pi.  17,  figs.  11, 

11  a.  Trenton. 

bela  Walcott,  1884;  35th  Rept.  New  York  State  Mus. Nat. Hist., p.  213, pi.  17, 

figs.  11, 11  a. 

buchiana  ? Jones,  1890 ; Quart.  Jour.  Geol.  Soc.,  vol.  46,  p.  16,  pi.  3,  fig.  25. 

Cincinnati. 

chambersi  Miller,  1874  ; Cincinnati  Quart.  Jour.  Sci.,  vol.  1,  p.  234,  fig.  27. 

Hudson. 

chambersi  Hall  and  Whitfield,  1875 ; Pal.  Ohio,  vol.  2,  p.  104,  pi.  4,  figs.  11, 12. 

ciliata  Emmons,  1855  ; American  Geology,  pt.  2,  p.  219,  fig.  74  c.  Hudson. 

ciliata  Miller,  1875;  Cincinnati  Quart.  Jour.  Sci.,  vol.  2,  p.  351. 

ciliata  Jones,  1890;  Quart.  Jour.  Geol.  Soc.,  vol.  46,  p.  19,  pi.  3,  figs.  12-16  ; pi.  4, 

figs.  16-18. 

Syn.,  Beyrichia  tumifrons  Hall. 

cincinnatiensis  Miller,  1875;  Cincinnnati  Quart.  Jour.  Sci.,  vol.  2,  p.  350,  fig.  25. 

Hudson. 


VOGDES  J 


CATALOGUE  OF  NON-TRILOBITES. 


159 


Beyrichia  cincinnatiensis  Walcott,  1876  ; Trans.  Albany  Inst.,  vol.  10,  p.  23. 

clarkei  Jones,  1890 ; Quart.  Jour.  Geol.  Soc.,  vol.  46,  p.  17,  wood-cut,  fig.  2. 

Lower  Helderberg. 

clathrata  Jones,  1858;  Annals  Mag.  Nat.  Hist.,  London,  3d  series,  vol.  1,  p.242, 

pi.  9,  fig.  1.  Niagara. 

dagon  Clarke,  1885 ; Bull.  U.  S.  Geol.  Survey,  No.  16,  p.  29,  pi.  2,  figs.  6, 7. 

Genesee. 

decora  Billings,  1866 ; Catalogue  Sil.  Foss.  Anticosti,  p.  67. 

duryi  Miller,  1874 ; Cincinnati  Quart.  Jour.  Sci.,  vol.  1,  p.  232,  figs.  24, 25. 

Hudson. 

fcetoidea  White  and  St.  John,  1868  ; Trans.  Chicago  Acad.  Sci.,  vol.  1,  p.  126,  figs. 

11  a,  b.  Niagara. 

granulosa  Hall,  1876 ; 28th  Rept.  New  York  State  Mus.  Nat.  Hist.,  Doc.  Ed.  Expl., 

pi.  32,  fig.  4.  Niagara. 

granulosa  Hall,  1876 ; 28th  Rept.  New  York  State  Mus.  Nat.  Hist.,  p.  186,  pi.  32, 

fig.  4. 

granulosa  Hall,  1883 ; 11th  Annual  Rept.  Dept.  Geol.  Nat.  Hist.  Indiana,  p.  331, 

pi.  34,  fig.  4. 

• granulosa  Jones,  1890;  Quart.  Jour.  Geol.  Soc.,  vol.  46,  p.  15,  pi.  1,  fig.  3. 

granulata  Hall,  1859;  Pal.  New  York,  vol.  3,  p.  377,  pi.  79  b,  figs.  1 a-d. 

Lower  Helderberg. 

halli  Jones,  1890;  Quart.  Jour.  Geol.  Soc.,  vol.  46,  p.  15,  pi.  4,  fig.  21. 

Waterlirae. 

hamiltonensis  Jones,  1890;  Quart.  Jour.  Geol.  Soc.,  vol.  46,  p.  19,  pi.  2,  fig.  3. 

Hamilton. 

jonesii  Dawson,  1868;  Acadian  Geology,  p.  313,  fig.  132.  Carboniferous. 

laid.  (See  Bollia  lata  Vanuxem.) 

lithof actor  White  and  St.  John,  Prelim.  Notice  New  Genera  and  Species  Foss., 

May  8,  1867,  p.  2. 

Changed  to  Beyrichia  petrifactor,  which  see.  Coal  Measures. 

lithofactor  var.  velata ; idem.,  p.  2.  (See  Beyrichia  petrifactor  var.  velata.) 

logani  Jones,  1858;  Annals  Mag.  Nat.  Hist.,  London,  3d  series,  vol.  1,  p.  244,  pi.  9, 

figs.  6-10.  Chazy. 

logani  Jones,  1858;  Geol.  Survey  Canada,  decade  3,  p.  91,  pi.  11,  figs.  1-5. 

logani  var.  remiformis  Jones,  1858;  Geol.  Survey  Canada,  decade  3,  p.  91,  pi. 

11,  fig.  1. 

logani  var.  leperditoides  Jones,  1858;  Geol.  Survey  Canada,  decade  3,  p.  91,  pi. 

11,  fig.  5. 

maccoyana  Jones,  1855;  Annals  Mag.  Nat.  Hist.,  London,  2d  series,  vol.  16,  p. 

88,  pi.  5,  fig.  14.  Onondaga. 

maccoyana  Jones,  1858 ; Annals  Mag.  Nat.  Hist.,  London,  3d  series,  vol.  1,  p.  252, 

pi.  10,  fig.  15. 

maccoyana  Jones,  1858;  Geol.  Survey  Penn.,  vol.  2,  p.  834,  fig.  695. 

notata.  (See  Klcedenia  notata  (Hall)  Jones.) 

nova  scotica  Jones  and  Kirkby,  1884;  Geol.  Mag.,  5th  series,  vol.  1,  p.  337,  pi. 

12,  figs.  5,  6.  Carboniferous. 

sp  ? Dawson,  1868;  Acadian  Geology,  p.  256,  fig.  78  c. 

[ Primitia ] occidentals  Walcott,  1884 ; Pal.  Eureka  Dist.,  Mon.  U.  S.  Geol.  Sur- 
vey, vol.  8,  p.  104,  pi.  17,  figs.  4,  4 a.  Devonian. 

oculifera  Hall,  1871 ; Pamphlet  Cincinnati  Group,  p.  8.  Hudson. 

oculifera  Hall,  1872;  24th  Rept.  New  York  State  Mus.  Nat.  Hist.,  p.  232,  pi.  8, 

figs.  9, 10. 

oculifera  Hall  and  Whitfield,  1875;  Pal.  Ohio,  vol.  2,  p.  103,  pi.  4,  figs.  9,  10. 

:J  oculifera  Miller,  1874;  Cincinnati  Quart.  Jour.  Sci.,  vol.  1,  p.  118. 

oculifera  Jones,  1890;  Quart.  Jour.  Geol.  Soc.,  vol.  46,  p.  21,  pi.  4,  figs.  19  a,  b,  20. 


160  A BIBLIOGRAPHY  OF  PALEOZOIC  CRUSTACEA.  [bull. 63. 

Beyrichia  oculina  Hall,  1859;  Pal.  New  York,  vol.  3,  p.  378,  pi.  79  b,  figs.  2 a-e. 

Lower  Helderberg. 

oculina  Jones,  1890;  Quart.  Jour.  Geol.  Soc.,  vol.  46,  p.  16,  pi.  1,  fig.  4. 

parasitica  (Hall)  Jones,  1890;  Quart.  Jour.  Geol.  Soc.,  vol.  46,  p.  16,  wood-cut. 

For  other  references,  see  Leperditia  parasitica . 

pennsylvanica  Jones,  1858;  Annals  Mag.  Nat.  Hist.,  London,  3d  series,  vol.  1, 

p.  253,  pi.  10,  fig.  16-18.  Onondaga. 

pennsylvanica  Jones,  1858;  Geol.  Survey  Penn.,  vol.  2,  p.  834,  fig.  696. 

persulcata  Ulrich,  1879;  Jour.  Cincinnati  Soc.  Nat.  Hist.,  vol.  2,  p.  12,  pi.  7, 

fig.  6.  Hudson. 

petrifactor  White  and  St.  John;  Trans.  Chicago  Acad.  Sci.,  vol.  1,  p.  125. 

petrifactor  var.  velata;  idem.,  p.  126. 

plagosa  Jones,  1858;  Annals  Mag.  Nat.  Hist.,  London,  3d  series,  vol.  1,  p.  243, 

pi.  9,  fig.  2.  Niagara. 

punctulifera  Hall,  1861 ; Des.  New  Species  Fossils,  p.  83.  Hamilton. 

punctulifera  Hall,  1862;  15th  Rept.  New  York  State  Cab.  Nat.  Hist.,  p.  111. 

pustulosa  Hall,  1860;  Canadian  Naturalist,  vol.  5,  p.  157,  fig.  19.  Silurian. 

pustulosa  Dawson,  1868 ; Acadian  Geology,  p.  608,  fig.  216. 

pustulosa  Jones,  1890;  Quart.  Jour.  Geol.  Soc.,  vol.  46,  p.  18,  pi.  2,  fig.  1 a-c. 

Referred  to  Beyrichia  tuherculata  Boll  var.  pustulosa  Hall. 

quadrilirata  Hall  and  Whitfield,  1875;  Pal.  Ohio,  vol.  2,  p.  105,  pi.  4,  figs.  6, 7. 

Hudson. 

quadrilirata  Miller,  1875;  Cincinnati  Quart.  Jour.  Sci.,  vol.  2,  p.  351.  (See 

Strepula  quadrilirata.) 

regularis  Emmons,  1855  ; American  Geology,  pt.  2,  p.  219,  fig.  74  b.  Hudson. 

regularis  Miller,  1875’;  Cincinnati  Quart.  Jour.  Sci.,  vol.  2,  p.  351. 

This  species  is  placed  as  a synonym  to  Bollia  lata  by  Jones  (1890,  Quart. 
Jour.  Geol.  Soc.,  vol.  46,  p.  13). 

remiformis  Jones,  1858;  Geol.  Survey  Canada,  decade  3,  p.  91,  pi.  11,  fig.  1. 

Chazy. 

richardsoni  Miller,  1874;  Cincinnati  Quart.  Jour.  Sci.,  vol.  1,  p.  347,  fig.  40. 

Hudson. 

rugulifera  Jones,  1858;  Annals  Mag.  Nat.  Hist.  London,  3d  series,  vol.  1,  p.  242, 

pi.  9,  fig.  4.  Niagara. 

sigillata  Jones,  1858;  Annals  Mag.  Nat.  Hist.,  London,  vol.  1,  p.  242,  pi.  9,  fig.  5. 

Niagara. 

simplex  (Jones)  Emmons,  1855 ; American  Geology,  vol.  1,  pt.  2,  p.  218,  fig.  74  a. 

{Cythei'ina']  spinosa  Hall,  1852;  Pal.  New  York,  vol.  2,  p.  317,  pi.  67,  figs.  17-20. 

(See  .ffichmina  spinosa.)  Niagara. 

striato-marginatus  Miller,  1874 ; Cincinnati  Quart.  Jour.  Sci.,  vol.  1,  p.  233,  fig. 

26. 

This  species  is  referred  to  a new  genus.  (See  Eurychilinda  striatomar- 

ginatus.)  Hudson. 

symmetrica  Hall,  1852;  Pal.  New  York,  vol.  2,  p.  317,  pi.  67,  fig.  16.  (See  Bollia 

symmetrica.)  Niagara. 

trisulcata  Hall,  1859 ; Pal.  New  York,  vol.  3,  p.  381,  pi.  79,  figs.  5 a,  b. 

Lower  Helderberg. 

trisulcata  Jones,  1890;  Quart.  Jour.  Geol.  Soc.,  vol.  46,  p.  14,  pi.  1,  fig.  2. 

tumifrons  Hall,  1871 ; Des.  New  Species  Foss.  Hudson  River  Group,  p.  7. 

Hudson. 

tumifrons  Hall,  1872 ; 24th  Rept.  New  York  State  Mus.  Nat.  Hist.,  p.  231,  pi.  8, 

fig.  11. 

tumifrons  Hall  and  Whitfield,  1875 ; Pal.  Ohio,  vol.  2,  p.  102,  pi.  4,  fig.  8. 

tumifrons  Miller,  1874;  Cincinnati  Quart.  Jour.  Sci.,  vol.  1,  p.  119. 

This  species  is  classed  by  Jones  1890,  Quart.  Jour.  Geol.  Soc.,  vol.  46,  p.  19, 
as  synonymous  to  Beyrichia  ciliata  Emmons. 


VOGUES. 


CATALOGUE  OF  N ON-TR1LOBXTES 


161' 


Beyrichia  venusta  Billings,  1866;  Catalogue  Silurian  Fossils  Anticosti,  p.  68. 
Bollia  Jones  aud  Holl,  1886;  Annals  Mag.  Nat.  Hist.,  5th  series,  London,  vol.  17,  p. 
360. 

\_Agnostu8']  latus  Vanuxem,  1842;  Geol.  New  York,  3d  Geol.  Dist.,p.  80. 

Clinton. 

[ Beyrichia ] lata  Hall,  1852;  Pal.  New  York,  vol.  2,  p.  301,  pi.  A 66,  figs.  10  a-c. 

[ Beyrichia ] lata  Jones,  1858;  Notes  on  Palaeozic  Entomostraca,  No.  2,  p.  168,  pi. 

6,  fig.  13. 

lata  Jones,  1800;  Quart.  Jour.  Geol.  Soc.,  vol.  46,  p.  12,  pi.  3,  figs.  1-3. 

[ Beyrichia ] symmetrica  Hall,  1852 ; Pal.  New  York,  vol.  2,  p.  317,  pi.  67,  fig.  16. 

Niagara. 

symmetrica  Jones,  1890 ; Quart.  Jour.  Geol.  Soc.,  vol.  46,  p.  12. 

This  species  is  closely  allied  to  Bollia  lata. 

ungula  (Claypole  MS.)  Jones,  1889;  American  Geologist,  vol.  4,  p.  338,  pi. 

fig.  10-13.  Marcellus. 

Bythocypris  Brady,  1880;  Challenger  Exped.,  Rep.  Ostracoda,  p.  45. 

cylindrica  (Hall)  Ulrich,  1889;  Contributions  Micro-Palseont.,  pt.  2,  p.  48,  pi. 

9,  fig.  6.  Trenton  and  Hudson. 

For  other  references,  see  Leperditia  \_Isochilina ] cylindrica  Hall. 

favulosa  Jones,  1889;  American  Geologist,  vol.  4,  p.  338,  pi.  figs.  2 a-c. 

Marcellus. 

oviformis  Jones,  1889 ; American  Geologist,  vol.  4,  p.  340,  pi.  figs.  3 a-c. 

Lower  Helderberg. 

Carbonia  Jones  and  Kirkby,  1879;  Annals  Mag.  Nat.  Hist.,  London,  5th  series, 
vol.  4,  p.  28. 

? bairdioides  (?)  Jones  and  Kirkby,  1884 ; Geol.  Mag.,  5th  series,  vol.  1,  p.  358, 

pi.  12,  figs.  8 a-d.  Carboniferous. 

Syn.,  Bairdia  sp.  ? Dawson,  1868;  Acadian  Geology,  p.  206,  figs.  48  a (?). 

[ Cyth ere ? (Carbonia)]  bairdiodes  Jones  and  Kirby,  1879 ; Annals  Mag.  Nat.  Hist., 

London,  5th  series,  vol.  4,  p.  38,  pi.  3,  figs.  24,  25. 

? bairdioides?  Jones  and  Kirkby,  1884;  Geol.  Mag.,  decade  3,  p.  358,  pi.  12, 

figs.  8 a-d. 

? elongata  Jones  and  Kirkby,  1884;  AnDals  Mag.  Nat.  Hist.,  London,  6th  series, 

vol.  1,  p.  361,  pi.  12,  fig.  10.  Carboniferous. 

? elongata  Jones  and  Kirkby,  1884;  Geol.  Mag.,  decade  3,  p.  361,  pi.  12,  fig.  10. 

fabulina  Jones  and  Kirkby,  1879;  Annals  Mag.  Nat.  Hist.,  London,  5th  series, 

vol.  4,  p.  31,  pi.  2,  figs.  1-9. 

fabulina  var.  humilis  Jones  and  Kirkby,  1879  ; Annals  Mag.  Nat.  Hist.,  London, 

5th  series,  vol.  4,  p.  31,  pi.  2,  figs.  11-14. 

fabulina  Jones,  1889;  Geol.  Mag.,  decade  3,  vol.  6,  p.  270,  figs.  1-4. 

[ Cytherilla ] injlata  Dawson,  1868;  Acadian  Geology,  p.  206,  fig.  48  b. 

fabulina  Jones  and  Kirkby,  1884;  Geol.  Mag.,  decade  3,  vol.  1,  p.  358,  pi.  12,  figs. 

9 a-e. 

Ceratiocaris  McCoy,  1849;  Annals  Mag.  Nat.  Hist.,  London,  vol.  4,  p.  412. 

aculeatus  Hall,  1859;  Pal.  New  York,  vol.  3,  p.  422"*,  pi.  80  a,  fig.  10.  Waterlimo. 

acuminatus  Hall,  1859 ; Pal.  New  York,  vol.  3,  p.  422*,  pi.  84,  fig.  6.  Waterlime. 

acuminatus  Pohlman,  1886 ; Bull.  Buffalo  Soc.  Nat.  Sci.,  vol.  5,  p.  28,  pi.  3,  fig.  2. 

annatus  Hall.  (See  Echinocaris  punctata.) 

beecheri  Clarke,  1881 ; Bull.  U.  S.  Geol.  Survey,  No.  16,  p.  44,  pi.  2,  fig.  1. 

Devonian. 

beecheri  Hall,  1888;  Pal.  New  York,  vol.  7,  p.  104,  pi.  31,  fig.  3. 

[ Colpocaris ] bradleyi  Meek,  1871  ; Proc.  Acad.  Nat.  Sci.  Phila.,  vol.  23,  p.  332. 

Lower  Carboniferous. 

[Onchus]  deweyi  Hall,  1852;  Pal.  New  York,  vol.  2,  p.  320,  pi.  71,  figs.  1 a-d. 

Niagara* 

Bull.  63 11 


162 


A BIBLIOGRAPHY  OF  PALEOZOIC  CRUSTACEA. 


[BULL.  63. 


Ceratiocaris  [ Colpocaris ] etytroides  Meek,  1871;  Proc.  Acad.  Nat.  Sci.  Phila.,  vol. 
23,  p.  334.  Lower  Carboniferous. 

grandis  Pohlman,  1881 ; Bull.  Buffalo  Soc.  Nat.  Sci.,  vol.  4,  p.  19,  fig.  5. 

Waterlime. 

longicaudus  Hall,  1863;  16tli  Rept.  New  York  State  Cab.  Nat.  Hist.,  p.  70,  pi.  1, 

fig.  7 ( not  figs.  4,  5,  6).  Hamilton. 

longicaudus  Packard,  1883 ; 12th  Annual  Rept.  U.  S.  Geol.  Survey  Territories, 

p.  450. 

longicaudus  Jones  and  Woodward,  1884;  Geol.  Mag.,  decade  3,  vol.  1,  p.  1. 

longicaudus  Etheridge,  Woodward,  and  Jones;  3d  Rept.  Comm.  Foss.  Phyllo- 

poda,  p.  35. 

longicaudus  Hall,  1888;  Pal.  New  York,  vol.  7,  p.  163,  pi.  31,  fig.  1. 

Not  C.  longicaudus  Clarke,  1885;  Bull.  U.  S.  Geol.  Survey,  No.  16,  p.  20. 

maccoyana  Hall,  1859;  Pal.  New  York,  vol.  3,  p.  421,  pi.  84,  figs.  1-5. 

Waterlime. 

f punctatus  Hall.  (See  Echinocaris  punctata.) 

— — simplex  Clarke,  1885 ; Bull.  U.  S.  Geol.  Survey,  No.  16,  p.  43,  pi.  2,  fig.  2. 

Devonian. 

— - ? simplex  Hall,  1888;  Pal.  New  York,  vol.  7,  p.  165,  pi.  31,  fig.  2. 

? sinuata  Meek  and  Worthen,  1868;  Am.  Jour.  Sci.,  2d  series,  vol.  46,  p.  22. 

Coal  Measures. 

? sinuata  Meek  and  Worthen,  1868;  Geol.  Survey  Illinois,  vol.  3,  p.  540,  fig.  a. 

[ Solenocaris ] strigata,  Meek,  1871;  Proc.  Acad.  Nat.  Sci.  Phila.,  vol.  23,  p.  335. 

Lower  Carboniferous. 

[ Solenocaris ] strigata  Meek,  1875 ; Pal.  Ohio,  vol.  2,  p.  321,  pi.  18,  figs.  4 a-c. 

The  generic  name  of  Solenocaris  was  used  by  Mr.  J.  Young  for  a genus  of 
the  Paleozoic  Crustacea  in  1868.  See  Strigocaris. 

Ciangopsis  Salter,  1863;  Name  changed  from  Palceocrangon. 

Cryptozoe  Packard,  1886 ; Proc.  Am.  Philos.  Soc.,  vol.  23,  p.  381. 

problematicus  Packard,  1886  ; Proc.  Am.  Philos.  Soc.,  vol.  23,  p.  382,  fig.  3,  plate. 

Carboniferous. 

Cyclus  De  Koninck,  1841 ; M6m.  Acad.  Sci.  Bruxelles,  vol.  14,  p.  18. 

americana  Packard,  1885 ; American  Naturalist,  vol.  19,  p.  293.  Coal  Measures. 

americana  Packard,  1886;  Mem.  Nat.  Acad.  Sci.,  vol.  3, p.  143,  pi.  5,  figs.  1,  1 a; 

pi.  6,  figs.  4,  4 a. 

Cythere  Muller,  1785;  Entomostraca,  p.  64. 

[ Beyrichia ] americana  Shumard,  1858;  TranB.  Acad.  Sci.  St.  Louis,  vol.  1,  p.  227. 

Upper  Coal  Measures. 

carbonaria  Hall.  (See  Leperditia  carbonaria.) 

cincinnatiensis  Meek.  (See  Entomis  cincinnatiensis.) 

crassimarginata  Winchell,  1862 ; Proc.  Acad.  Nat.  Sci.  Phila.,  p.  429.  Marshall. 

irregularis  Miller,  1878;  Jour.  Cincinnati  Soc.  Nat.  Hist.,  vol.  1,  p.  106,  pi.  3,, 

figs.  7,  7 a.  Hudson.. 

nebrascensis  Geinitz,  1866  ; Carb.  und  Dyas  in  Nebraska,  p.  2,  pi.  1,  fig.  2. 

Coal  Measures. 

nebrascensis  Meek,  1872 ; Rept.  U.  S.  Geol.  Survey  Territories,  Final  Report 

Nebraska,  p.  237,  pi.  11,  figs.  1,2,3  a,  b (?). 

nebrascensis  Keyes,  1888;  Proc.  Acad.  Nat.  Sci.  Phila.,  p.  222. 

ohiones  Herrick,  1889;  Bull.  Den.  Univ.,  vol.  4,  p.  60,  pi.  8,  fig.  8;  vol.  3,  pi.  3, 

fig.  19.  Kinderhook. 

ohiones  Herrick,  1890 ; American  Geologist,  vol.  4,  p.  254. 

okeni.  (See  Leperditia  okeni.) 

simplex  White  and  St.  John,  1867  ; Prelim.  Notice  New  Species  Foss.,  p.  3. 

St.  Louis. 

simplex  White  and  St.  John,  1868;  Trans.  Chicago  Acad.  Sci.,  vol,  1,  p.  127. 


VOGDES.J 


CATALOGUE  OF  NON-TRILOB1TES. 


163 

Carboniferous. 


Cythere  sp.  ? Dawson,  1868 ; Acadian  Geology,  p.  256,  fig.  78  a. 

sublcevis.  (See  Leperditia  sublaevis. ) 

subrecta.  (See  Leperditia  subrecta.) 

Cytherina  Lamarck,  1818;  Animaux  sans  Vert.,  vol.  5,  p.  125. 

alia.  (See  Leperditia  alta.) 

crenulata  Emmons,  1855 ; Am.  Geology,  vol.  1,  p.  221,  figs.  75  a-d.  Trenton. 

cylindrica.  (See  Isochilina  cylindrica.) 

emmonsi  Vogdes,  1889 ; Annals  N.  Y.  Acad.  Sci.,  vol.  5,  p.  13,  to  replace  C.  sub- 

cylindrica. 

spinosa.  (See  Beyrichia  spinosa.) 

subcylindrica  Emmons,  1855;  Am.  Geology,  vol.  1,  p.  220,  fig.  75  b.  Trenton. 

This  name  was  used  by  Munster  for  a species  of  this  genus.  Change  to  C. 
emmonsi. 

subelliptica  Emmons,  1855;  Am.  Geology,  vol.  1,  p.  220,  figs.  75  a. 

Trenton. 

Cytherellina  Jones  and  Holl,  1869 ; Annals  Mag.  Nat.  Hist.,  London,  4th  series,  vol. 
3,  p.  215. 

grandella  Whitfield,  1882 ; Bull.  Am.  Mus.  Nat.  Hist.  New  York,  vol.  1,  p.  94, 

pi.  9,  figs.  28, 29.  Warsaw. 

Cytheropsia  McCoy,  1855  ; Synopsis  Classification  Brit.  Pal.  Rocks,  pi.  1 L.,  fig.  2. 
No  definite  descriptign  of  the  genus  given. 

concinna  Jones.  (See  Primitia  concinna.) 

rugosa  Jones.  (See  Primitia  rugosa.) 

silique  Jones,  1858 ; Annals  Mag.  Nat.  Hist.,  3d  series,  London,  vol.  1,  p.  249, 

pi.  10,  fig.  6.  Trenton. 

silique  Jones,  1858 ; Geol.  Survey  Canada,  decade  3,  p.  99. 

silique  Jones,  1869 ; Annals  Mag.  Nat.  Hist.,  London,  4th  series,  vol.  3,  p.  216, 

pi.  14,  figs.  1-6. 

Dipeltis  Packard,  1885;  Am.  Naturalist,  vol.  19,  p.  293. 

diplodiscus  Packard,  1885;  Am.  Naturalist,  vol.  19,  p.  293.  Carboniferous. 

diplodiscus  Packard,  1886;  Mem.  Nat.  Acad.  Sci.,  vol.  3,  p.  145,  pi.  5,  figs.  2,2  a. 

Diplostylus  Salter,  1863 ; Quart.  Jour.  Geol.  Soc.  London,  vol.  19,  p.  76. 

dawsoni  Salter,  1863 ; Quart.  Jour.  Geol.  Soc.  London,  vol.  19,  p.  77,  fig.  6. 

Coal  Measures. 

Dipterocaris  Clarke,  1883 ; Am.  Jour.  Sci.,  3d  series,  vol.  25,  p.  121. 

pennae-daedali  Clarke,  1883 ; Am.  Jour.  Sci.,  3d  series,  vol.  25,  p.  122,  fig.  1. 

Chemung. 

pennae-daedali  Jones  and  Woodward,  1884 ; Geol.  Mag.,  decade  3,  vol.  1,  p.  349. 

pennae-daedali  Etheridge,  Woodward,  and  Jones,  1884 ; 2d  Kept.  Comm.  Foss. 

Phyllopoda  Pal.  Rocks,  p.  11. 

pennae-daedali  Etheridge,  Woodward,  and  Jones,  1885 ; 3d  Rept.  Comm.  Foss. 

Phyllopoda  Pal.  Rocks,  p.  3. 

pennae-daedali  Hall,  1888  ; Pal.  New  York,  vol.  7,  p.  200,  pi.  35,  fig.  24. 

pennae-daedali  Etheridge,  Woodward,  and  Jones,  1888;  6th  Rept.  Comm.  Foss. 

Phyllopoda  Pal.  Rocks,  p.  9. 

percervae  Clarke,  1883 ; Am.  Jour.  Sci.,  3d  series,  vol.  25,  p.  123,  figs.  4,5. 

Chemung. 

percervae  Jones  and  Woodward,  1884  ; Geol.  Mag.,  decade  3,  vol.  1,  p.  349. 

percervae  Etheridge,  Woodward,  and  Jones,  1884 ; 2d  Rept.  Comm.  Foss.  Phyllo- 

lopoda  Pal.  Rocks,  p.  11. 

percervae  Etheridge,  Woodward,  and  Jones,  1885  ; 3d  Rept.  Comm.  Foss.  Pbyllo- 

poda  Pal.  Rocks,  p.  3. 

percervae  Hall,  1888  ; Pal.  New  York,  vol.  7,  p.  202,  pi.  35,  figs.  20, 21. 

percervae  Etheridge,  Woodward,  and  Jones,  1888;  6th  Rept.  Comm,  Foss,  Phyllo- 
poda Pal.  Rocks,  p.  9. 


164 


[BULL.  63. 


A BIBLIOGRAPHY  OF  PALEOZOIC  CRUSTACEA. 

Dipterocaris  prcene  Clarke,  1883  ; Am.  Jour.  Sci.,  3d  series,  vol.  25,  p.  122,  figs.  2,  3. 

Chemung. 

prcene  Jones  and  Woodward,  1884;  Geol.  Mag.,  decade  3,  vol.  1,  p.  349. 

prcene  Etheridge,  Woodward,  and  Jones,  1884 ; 2d  Rept.  Comm.  Foss.  Phyllo- 

poda  Pal.  Rocks,  p.  11. 

prcene  Etheridge,  Woodward,  and  Jones,  1885 ; 3d  Rept.  Comm.  Foss.  Phyllo- 

poda  Pal.  Rocks,  p.  3. 

prcene  Hall,  1888 ; Pal.  New  York,  vol.  7,  p.  201,  pi.  35,  figs.  25-27. 

prcene  Etheridge,  Woodward,  and  Jones,  1888  ; 6th  Rept.  Comm.  Foss.  Phyllo- 

pod  a Pal.  Rocks,  p.  9. 

Dithyrocaris  (Scouler,  1843,  MS.)  Portlock,  1843;  Rept.  Geol.  Londonderry,  etc.,  p. 
313. 

belli  Woodward,  1870;  Geol.  Mag.,. decade  2,  vol.  8,  p.  106,  pi.  3,  figures. 

Devonian. 

belli  Etheridge,  Woodward,  and  Jones,  1887 ; 5th  Rept.  Comm.  Foss.  Phyllo- 

poda  Pal.  Rocks,  p.  6. 

belli  Hall,  1888 ; Pal.  New  York,  vol.  7,  p.  194. 

carbonaria  Meek  and  Worthen,  1870  ; Proc.  Acad.  Nat.  Sci.  Phila.,  vol.  22,  p.  55. 

Coal  Measures. 

carbonaria  Meek  and  Worthen,  1873  ; Geol.  Survey  Illinois,  vol.  5,  p.  6! 8,  pi. 

32,  fig.  1. 

carbonaria  White,  1884  ; 13th  Rept.  Dept.  Geol.  Nat.  Hist.  Indiana,  p.  178,  pi. 

39,  fig.  2. 

neptuni  Hall.  (See  Mesothyra  neptuni.) 

DolichocepliaJa  Claypole,*1883 ; Proc.  Am.  Philos.  Soc.,  vol.  21,  p.  236. 

locoanci  idem ; p.236, plate.  (See  Stylonurus  excelsior.) 

Dolichopterus  (subgenus  Eurypterus)  Hall,  1859;  Pal.  New  York,  vol.  3,  p.  414. * 

macrocheous  Hall,  1859 ; Pal.  New  York,  vol.  3,  p.  414,*  pi.  83,  fig.  1 ; pi.  83  a,  fig.  1. 

Waterlime. 

Echinocaris  Whitfield,  1880 ; Am.  Jour.  Sci.,  3d  series,  vol.  19,  p.  34. 

condylepsis  Hall,  1888 ; Pal.  New  York,  vol.  7,  p.  173,  pi.  19,  figs.  14-17. 

Chemung. 

multinodosa  Whitfield,  1880 ; Am.  Jour.  Sci. , 3d  series,  vol.  19,  p.  38,  fig.  8.  (Plates 

with  author’s  special  edition  only.)  Erie  Shales. 

multinodosa  Packard,  1882 ; Am,  Naturalist,  vol.  16,  p.  952,  fig.  10. 

multinodosa  Packard,  1883 ; 12th  Rept.  U.  S.  Geol.  Survey  Territories,  p.  451, 

fig.  71  a. 

multinodosa  Beecher,  1884  ; 2d  Geol.  Survey  Penn.,  vol.  PPP,  p.  5. 

multinodosa  Etheridge,  Woodward,  and  Jones,  1885 ; 3d  Rept.  Comm.  Foss. 

Phyllopoda  Pal.  Rocks,  p.  35. 

multinodosa  Hall,  1888 ; Pal.  New  York,  vol.  7,  p.  180,  pi.  29,  figs.  18-19. 

multinodosa  Etheridge,  Woodward,  and  Jones,  1888;  6th  Rept.  Comm.  Foss. 

Phyllopoda  Pal.  Rocks,  p.  8. 

[ Ceratiocaris]  punctatus  Hall,  1863;  16th  Rept.  New  York  State  Cab.  Nat.  Hist. 

p.  74,  pi.  1,  fig.  8.  Hamilton. 

punctatus  Whitfield,  1880;  Am.  Jour.  Sci.,  3d  series,  vol.  19,  p.  39. 

Syn.,  Ceratiocaris  armatus  Hall,  1863;  16th  Rept.  New  York  State  Cab.  Nat. 
Hist.,  p.  72,  pi.  1,  figs.  1-3. 

Ceratiocaris  armatus  Hall,  1876;  Illus.  Devonian  Foss.,  pi.  23,  figs.  4,5. 

[ Ceratiocaris  ( Aristozoe)]  punctatus  Hall,  1876;  Illus.  Devonian  Foss.,.Expl. 

pi.  23,  fig.  7. 

punctatus  Packard,  1882;  Am.  Naturalist,  vol.  16,  p.952,  fig.  12. 

punctatus  Packard,  1883 ; 12th  Rept.  U.  S.  Geol.  Survey  Territories,  p.  450,. 

fig.  70. 

Syn.,  armatus  Packard,  1883  ; 12th  Rept.  U.  S.  Geol.  Survey  Terri tories^p.  451. 


vogdes.]  CATALOGUE  OF  NON-TRILOBITES.  165 

Echinocaris  punctatus  Beecher,  1884 ; 2d  Geol.  Survey  Penn.,voI.  PPP,  p.  6,  pi.  1, 
figs.  13-16 ; also  fig.  1 in  text,  page  4. 

Syn.,  armatus  Jones  and  Woodward,  1884;  Geol.  Mag., decade  3,  vol.  1,  p.  2,  pi. 

13,  fig.  2. 

armatus  Etheridge,  Woodward,  and  Jones,  1885;  3d  Rept.  Comm.  Foss. 

Phyllopoda  Pal.  Rocks,  p.  35. 

punctatus  Hall,  1888;  Pal.  New  York,  vol.  7,  p.  166,  pi.  27,  fig.  10  ; pi.  28,  fig.  1-7 ; 

' pi.  29,  fig.  1-8. 

punctatus  Etheridge,  Woodward,  and  Jones,  1888;  6th  Rept.  Comm.  Foss. 

Phyllopoda  Pal.  Rocks,  p.  8. 

.pustulosa  Whitfield,  1880 ; Am.  Jour.  Sci.,  3d  series,  vol.  19,  p.  38,  pi.  fig.  7 

(plate  with  author’s  special  edition  only).  Erie  Shales. 

pustulosa  Packard,  1883  ; 12th  Rept.  U.  S.  Geol.  Survey  Territories,  p.  451. 

pustulosa  Beecher,  1884 ; 2d  Geol.  Survey  Penn.,  vol.  PPP.,  p.  5. 

pustulosa  Jones  and  Woodward,  1884  ; Geol.  Mag.,  decade  3,  vol.  1,  p.  2,  pi.  13, 

fig.  6. 

pustulosa  Etheridge,  Woodward,  and  Jones,  1885;  3d  Rept.  Comm.  Foss- 

Phyllopoda  Pal.  Rocks,  p.  35. 

pustulosa  Hall,  1888 ; Pal.  New  York,  vol.  7,  p.  178,  pi.  29,  figs.  9,  10. 

pustulosa  Etheridge,  Woodward,  and  Jones,  1888;  6th  Rept.  Comm.  Foss. 

Phyllopoda  Pal.  Rocks,  p.  8. 

socialis  Beecher,  1884 ; 2d  Geol.  Survey  Penn.,  vol.  PPP,  p.  10,  pi.  1,  figs.  1- 

le.  Chemung. 

socialis  Etheridge,  Woodward,  and  Jones,  1885 ; 3d  Rept.  Comm.  Foss.  Phvllo. 

poda  Pal.  Rocks,  p.  35. 

socialis  Hall,  1888 ; Pal.  New  York,  vol.  7,  p.  174,  pi.  30,  figs.  1-12. 

socialis  Etheridge,  Woodward,  and  Jones,  1888;  6th  Rept.  Comm.  Foss.  Phyllo- 
poda Pal.  Rocks,  p.  8. 

sublevis  Whitfield,  1880 ; Am.  Jour.  Sci.,  3d  series,  vol.  19,  p.  36,  pi.  figs.  4-6 

(plate  with  the  authors  special  edition  only).  Erie  Shales. 

sublevis  Packard,  1882;  Am.  Naturalist,  vol.  16,  p.  952,  fig.  11. 

sublaevis  Packard,  1883;  12th  Rept.  U.  S.  Geol.  Survey  Territories,  p.  450,  fig. 

71  b. 

sublevis  Beecher,  1884;  2d  Geol.  Survey  Penn.,  vol.  PPP,  p.  5. 

sublaevis  Jones  and  Woodward,  1884 ; Geol.  Mag., decade  3,  vol.  1.  p.  2,  pi.  13,  figs. 

3,  4,  5. 

sublaevis  Etheridge,  Woodward,  and  Jones,  1885;  3d  Rept.  Comm.  Foss.  Phyllo- 
poda Pal.  Rocks,  p.  35. 

sublaevis  Hall,  1888;  Pal.  New  York,  vol.  7,  p.  176,  pi.  29,  figs.  11-13. 

sublaevis  Etheridge,  Woodward,  and  Jones,  1888 ; 6th  Rept.  Comm.  Foss.  Phyl- 
lopoda Pal.  Rocks,  p.  8. 

whitfieldi  Clarke,  1885 ; Bull.  U.  S.  Geol.  Survey,  No.  16,  p.  45,  pi.  2,  figs.  3,  4. 

Portage. 

whitfieldi  Hall,  1888;  Pal.  New  York,  vol.  7,  p.  172,  pi.  29,  figs.  20,  21. 

whitfieldi  Etheridge,  Woodward,  and  Jones,  1888;  6th  Rept.  Comm.  Foss.  Phyl- 
lopoda Pal.  Rocks,  p.  8. 

Echinognathus  Walcott,  1882;  Am.  Jour.  Sci.,  3d  series,  vol.  23,  p.  213. 

clevelandi  Walcott,  1882 ; Am.  Jour.  Sci.,  3d  series,  vol.  23,  p.  213,  figs.  1,  2. 

Utica. 

[ Eurypterus  ?]  clevelandi  Walcott,  1882;  Am.  Jour.  Sci.,  3d  series,  vol.  23,  p.  151. 

Elymocaris  Beecher,  1884;  2d  Geol.  Survey  Penu.,  vol.  PPP,  p.  13. 

siliqua  Beecher,  1884 ; 2d  Geol.  Survey  Penn.,  vol.  PPP,  p.  13,  pi.  2,  figs.  1,  2. 

Chemung. 

siliqua  Etheridge,  Woodward,  and  Jones,  1885;  3d  Rept.  Comm.  Foss.  Phyllo- 
poda Pal.  Rocks,  p.  35. 


166  A BIBLIOGRAPHY  OF  PALEOZOIC  CRUSTACEA.  [bull.63. 

Elymocaris  siliqua  Hall,  1888;  Pal.  New  York,  vol.  7,  p.  182,  pi.  31,  figs.  5,  6. 

siliqua  Etheridge,  Woodward,  and  Jones,  1888;  6th  Rept.  Comm.  Foss.  Phyllo- 

poda  Pal.  Rocks,  p.  8. 

Entomis  Jones,  1861 ; Mem.  Geol.  Survey  Scotland,  Expl.  Map  32,  p.  137 ; also,  An- 
nals Mag.  Nat.  Hist.,  London,  4th  series,  vol.  11,  p.  413. 

[ Cythere ] cincinnatiensis  Meek,  1871 ; Proc.  Acad.  Nat.  Sci.  Phila.,  vol.  23,  p.  331. 

Hudson. 

[Cythere ] cincinnatiensis  Meek,  1873;  Pal.  Ohio,  vol.  1,  p.  158,  pi.  14,  figs.  1 a- 

1 d. 

[ Cythere ] cincinnatiensis  Miller,  1874;  Cincinnati  Quart.  Jour.  Sci.,  vol.  1,  p. 

120. 

cincinnatiensis  Jones,  1884;  Annals.  Mag.  Nat.  Hist.,  London,  5th  series,  vol. 

14,  note  p.  395. 

rhomboidea  Jones,  1890 ; Quart.  Jour.  Geol.  Soc.,  vol.  46,  p.  10,  pi.  2,  figs.  9, 10  a,  b. 

Hamilton. 

Equisetides  wrightiana.  This  species  is  referred  by  Woodward  and  Jones  (3d  Report 
Comm.  Foss.  Phyllopoda  Brit.  Assoc.,  1885,  p.  360)  to  Echinocaris.  Prof.  James 
Hall  places  it  provisionally  with  Stylonurus,  which  see. 

Estheria  Ruffell,  1857 ; Mus.  Senckenberg,  vol.  2,  p.  119. 

dawsoni  Jones,  1870;  Geol.  Mag.,  vol.  7,  p.  220,  pi.  9,  fig.  15.  Carboniferous. 

dawsoni  Jones,  1878;  Geol.  Mag.,  decade  2,  vol.  2,  p.  101,  pi.  3,  fig.  2. 

sp.  ? Dawson,  1868 ; Acadian  Geology,  p.  256,  fig.  78  d. 

dawsoni  Jones  and  Kirkby,  1884 ; Geol.  Mag.,  decade.  3,  voi.  1,  p.  361,  pi.  12,  fig.  12. 

pulex  Clarke,  1882;  Am.  Jour.  Sci.,  3d  series,  vol.  23,  p.  476,  pi.,  fig.  4. 

Hamilton. 

pulex  Packard,  1883 ; 12th  Rept.  U.  S.  Geol,  Survey  Territories,  p.  355. 

pulex  Etheridge,  Woodward,  and  Jones,  1885;  5th  Rept.  Comm.  Foss.  Phyllo- 
poda Pal.  Rocks,  p.  10. 

pulex  Hall,  1888;  Pal.  New  York,  vol.  7,  p.  206,  pi.  35,  figs.  10, 11. 

pulex  Etheridge,  Woodward,  and  Jones,  1888;  6th  Rept.  Comm.  Foss.  Phyllo- 
poda Pal.  Rocks,  p.  9. 

Euproops  Meek,  1867 ; Am.  Jour.  Sci.,  2d  series,  vol.  34,  p.  394.  (See  Bellinurus  and 
Frestwichia.) 

Eurychilinda  Ulrich,  1889;  Contributions  Micro-Palseont.,  pt.  2,  p.  52. 

mantiobensis  Ulrich,  1889;  Contributions  Micro-Palseont.,  pt.  2,  p.  53,  pi.  9, 

figs.  10,  10  a.  Hudson. 

reticulata  Ulrich,  1889;  Contributions  Micro-Palseont.,  pt.  2,  p.  52,  pi.  9,  figs. 

9,  9 a.  Trenton. 

striato-marginata  (Miller)  Ulrich,  1889;  Contributions  Micro-Palseont.,  pt.  2, 

p.  52. 

For  other  references,  see  Beyrichia  striato-marginata. 

Eurypterus  De  Kay,  1825;  Annals  Lyceum  Nat.  Hist.  N.  Y.,  vol.  1,  pt.  2,  p.  375. 

beecheri  Hall,  1884 ; 2d  Geol.  Survey  Pennsylvania,  vol.  PPP,  p.  30,  pi.  3,  fig.  1. 

Chemung. 

beecheri  Hall,  1888 ; Pal.  New  York,  vol.  7,  p.  156,  pi.  27,  fig.  5. 

beecheri  Etheridge,  Woodward,  and  Jones,  1888 ; 6th  Rept.  Comm.  Fossil  Phyllo- 
poda Pal.  Rocks,  p.  9. 

boylei  Whiteaves,  1884 ; Pal.  Fossils,  vol.  3,  pt.  1,  p.  42,  pi.  7,  fig.  3.  Guelph. 

dekayi  Hall,  1859 ; Pal.  New  York,  vol.  3,  p.  411*,  pi.  82,  fig.  1.  Waterlime. 

eriensis  Whitfield,  1881 ; Annals  New  York  Acad.  Sci.,  vol.  2,  p.  196. 

Lower  Helderberg. 

giganteus  Pohlman,  1882;  Bull.  Buffalo  Soc.  Nat.  Sci.,  vol.  4,  p.  41,  pi.  2,  fig.  1. 

Waterlime. 

lacustriB  Harlan,  1834;  Trans.  Geol.  Soc.  Pennsylvania,  vol.  l,p.  98,  pi.  5,  fig.  2. 

Waterlime. 


V0GDE8.  J 


CATALOGUE  OF  NON-TRILOBITES. 


167 


Eurypterus  lacustris  Harlan,  1835 ; Med.  Phys.  Researches,  p.  297,  plate,  fig.  2. 

lacustris  Hall,  1859;  Pal.  New  York,  vol.  3,  p.  407*,  pi.  81,  figs.  1-11;  pi.  81  a, 

fig.  1 ; pi.  81  b,  figs.  1-5 ; pi.  83  b,  fig.  3 ; also  fig.  5 in  text  p.  400*. 

lacustris  var.  robustus  Hall,  1859 ; Pal.  New  York,  vol.  3,  p.  410*,  pi.  81  c,  fig.  2. 

[ Dolichopterus ] mansfieldi  Hall,  C.  E.,1877;  Proc.  Am.  Philos.  Soc.,  vol.  16, 

p.  621.  Carboniferons. 

mansfieldi  Hall,  1884 ; 2d  Geol.  Survey  Pennsylvania,  vol.  PPP,  p.  32,  pi.  4, 

figs.  1-8;  pi.  5,  figs.  1-11 ; pi.  6,  fig.  1 ; pi.  7,  fig.  1 ; pi.  8,  figs.  1-3. 

[ Anthraconectes ] mazonensis  Meek  and  Worthen,  1868;  Am.  Jour.  Sci.,  2d 

series,  vol.  46,  p.  21.  Coal  Measures. 

[ Anthraconectes ] mazonensis  Meek  and  Worthen,  1868 ; Geol.  Survey  Illinois, 

vol.  3,  p.  544,  figures. 

— — [Anthraconectes']  mazonensis  Hall,  1884;  2d  Geol.  Survey  Pennsylvania,  vol. 
PPP,  p.  25,  fig.  2;  p.  27,  fig.  3. 

[ Anthraconectes ] mazonensis  White,  1884 ; 13th  Ann.  Rept.  Dept.  Geol.  Nat. 

Hist.  Indiana,  p.  168,  pi.  37,  figs.  1,  2,  3. 

microphthalmus  Hall,  1859;  Pal.  New  York,  vol.  3,  p.  407*,  pi.  80  a,  fig.  7. 

Lower  Helderberg. 

pachycheirus  Hall,  1859 ; Pal.  New  York,  vol.  3,  p.  412*,  pi.  8,  figs.  1-3. 

Waterlime. 

pennsylvanicus  Hall,  C.  E.,  1877 ; Trans.  Am.  Philos.  Soc.  Phila.,  vol.  7,  p.  621. 

Carboniferous. 

pennsylvanicus  Hall,  1884 ; 2d  Geol.  Survey  Pennsylvania,  vol.  PPP,  p.  31, 

pi.  5,  fig.  18. 

pohlmani  Vogdes,  1889 ; to  take  the  place  of  the  preoccupied  name  of  E.  scor- 

piovis  Grote  and  Pitt.  Ann.  N.  Y.  Acad.  Sci.,  vol.  5,  No.  1. 

potens  Hall,  1884 ; 2d  Geol.  Survey  Pennsylvania,  vol.  PPP,  pi.  4,  figs.  9, 10. 

Carboniferous. 

prominens  Hall,  1884  ; Proc.  Am.  Assoc.  Adv.  Sci.,  vol.  33,  p.  420.  Clinton. 

prominens  Hall,  1888;  Pal.  New  York,  vol.  7,  p.  157,  pi.  27,  figs.  3,  4. 

pulicaris  Salter,  1863;  Quart.  Jour.  Geol.  Soc.  London,  vol.  19,  p.  78,  figs.  9, 10. 

Coal  Measures. 

pulicaris  Dawson,  1868 ; Acadian  Geology,  p.  523,  figs.  179  a,  b. 

pustulosus  Hall,  1859 ; Pal.  New  York,  vol.  3,  p.  413*,  pi.  83  b,  fig.  1. 

Waterlime. 

remipes  De  Kay.  Waterlime. 

Syn.,  Fossil  Fish  Mitchell,  1818;  Am.  Monthly  Mag.,  vol.  3,  p.  291. 

remipes  De  Kay,  1825;  Annals  Lyceum  Nat.  Hist.,  vol.  1,  p.  375,  pi.  29. 

remipes  Harlan,  1834 ; Trans.  Geol.  Soc.  Penn.,  vol.  1,  p.  96,  pi.  5. 

remipes  Harlan,  1835;  Medical  Phys.  Researches,  p.  297,  pi.,  fig.  1. 

remipes  Milne-Ed  wards,  1840;  Hist.  Nat.  Crust.,  vol.  3,  p.  422. 

remipes  Burmeister,  1843;  Org.  Trilobiten,  p.  62  (Ray  Soc.  ed.,  p.  54). 

remipes  Bronn,  1837 ; Lethea  Geognostica,  vol.  1,  p.  666,  pi.  9s,  fig.  1 ; pi.  9,  fig.  1. 

remipes  Salter,  1859 ; Quart.  Jour.  Geol.  Soc.  London,  vol.  15,  p.  255. 

remipes  Nieszkowski,  1858;  Der  Eurypterus  remipes,  etc.,  pis.  1,  2,  3. 

remipes  Hall,  1859 ; Pal.  New  York,  vol.  3,  p.  404,  pi.  80,  figs.  1-12 ; pi.  80  a, 

figs.  1-6;  pi.  83  b,  fig.  2,  also  p.  403*,  figs.  6,  7. 

remipes  (numerous  authors). 

[Eusarcus]  grandis  Grote  and  Pitt,  1875 ; Bull.  Buffalo  Soc.  Nat.  Sci.,  vol.  3,  p.  17. 

Waterlime. 

Referred  by  J.  Pohlman  (Bull.  Buffalo  Soc.  Nat.  Sci.,  vol.  5,  p.  31)  to 
Eurypterus  scorpionia.  An  almost  similar  terra,  E.  scorpioides  was  used  for  a 
species  of  this  genus  by  H.  Woodward  in  1868;  I suggest  that  of  E.  pohlmani 
for  this  species. 

[ Eu8arcu8~\  scorpionis  Grote  and  Pitt,  1875;  Bull.  Buffalo  Soc.  Nat.  Sci.,  vol.  3, 

pp.  1,  17,  photographic  plate.  Waterlime. 


168 


A BIBLIOGRAPHY  OF  PALEOZOIC  CRUSTACEA. 


(BULL.  63. 


Eurypterus  [ Eusarcus ] scorpionis  (Grote  and  Pitt)  Pohlman,  1886;  Bull.  Buffalo 
Soc.  Nat.  Sci.,  vol.  5,  p.  30,  pi.  2,  fig.  3. 

[ Eusarcus ] grandis  (Grote  and  Pitt)  Pohlman,  1886;  Bull.  Buffalo  Soc.  Nat.  Sci., 

vol.  5,  p.  31. 

Referred  to  Eurypterus  pohlmani  Vogdes,  1889;  Annals  N.  Y.  Acad.  Sci.,  vol.  5, 

p.  22. 

Hymenocaris  Salter,  1853 ; 22dRept.  Brit.  Assoc.  Adv.  Sci.,  Trans,  of  sec.,  p.  56. 
Isochilina  Jones,  1857 ; Mem.  Geol.  Survey  Canada,  decade  3,  p.  97. 

^Leperditia  ( Isochilina )]  armata  Walcott,  1883;  Des.  New  Sp.  Foss.  Trenton 

Group,  p.  7. 

\_Leperditia  ( Isochilina )]  armata  Walcott,  1884 ; 35th  Rept.  N.  Y.  State  Mus.  Nat. 

Hist.,  p.  213. 

cristata  (Whitfield)  Jones,  1890;  Quart.  Jour.  Geol.  Soc.,  vol.  46,  p.  23,  pi..  1, 

fig.  8.  Calciferous. 

For  other  references,  see  Primitia  cristata. 

[ Cyilierina ] cylindrica  Hall,  1852;  Pal.  New  York,  vol.  2,  p.  14,  pi.  4,  figs.  8 a,  b. 

Medina. 

Prof.  T.  Rupert  Jones  (Quart.  Jour.  Geol.  Soc.,  vol.  46,  1890,  p.  8)  refers  this 

species  to  Leperditia  cylindrica. 

\_Leperditia  ( Isochilina )]  cylindrica  Jones,  1858;  Annals  Mag.  Nat.  Hist.,  3d 

series,  vol.  1,  p.  253 ; also,  Geol.  Survey  Canada,  decade  3,  p.  101. 

[ Leperditia  ( Isochilina )]  cylindrica  Hall,  1871 ; Description  n.  sp.  Fossils  Hud- 
son River  Group. 

[ Leperditia  ( Isochilina )]  cylindrica  Hall,  1872;  24th  Rept.  N.  Y.  State  Mus.  Nat. 

Hist.,  p.  231,  pi.  8,  $g.  2;  also,  Pal.  Ohio,  vol.  2, 1875,  p.  101,  pi.  4,  fig.  5. 

Prof.  T.  Rupert  Jones  (Quart.  Jour.  Geol.  Soc.,  vol.  46,  1890,  p.  8)  refers  this 
species  to  Primitia  minuta  Eichwald. 

cylindrica  Miller,  1875 ; Cincinnati  Quart.  Jour.  Sci.,  vol.  2,  p.  351. 

fabacea  Jones,  1890 ; Quart.  Jour.  Geol.  Soc.,  vol.  46,  p.  22,  pi.  2,  fig.  11. 

Hamilton. 

[ Leperditia  ( Isochilina )]  gracilis  Jones,  1858;  Annals  Mag.  Nat.  Hist.,  London, 

3d  series,  vol.  1,  p.  248,  pi.  10,  fig.  2;  also,  Geol.  Survey  Canada,  decade  3,  p.  98, 
pL  2,  fig.  15.  Trenton. 

gregaria  (Whitfield)  Jones,  1890 ; Quart.  Jour.  Geol.  Soc.,  vol.  46,  p.  22,  pi.  1,  figs. 

9, 10. 

For  other  references,  see  Primitia  gregaria. 

jonesi  Wetherby,  1881 ; Jour.  Cincinnati  Soc.  Nat.  Hist.,  vol.  4,  p.  80,  pi.  2,  figs. 

7,  7 a.  Subcarboniferous. 

lineata  Jones,  1890 ; Quart.  Jour.  Geol.  Soc.,  vol.  46,  p.  21,  pi.  2,  figs.  5 a,  b,  8 a,  b. 

Hamilton. 

[ Leperditia  ( Isochilina )]  minutissima  Hall,  1871 ; Des.  New  Species  Foss.  Hud- 
son River  Group,  p.  7. 

[ Leperditia  ( Isochilina )]  minutissima  Hall,  1872;  24th  Rept.  New  York  State 

Mus.  Nat.  Hist.,  p.  231,  pi.  8,  fig.  13. 

[ Leperditia  ( Isochilina )]  minutissima  Hall  and  Whitfield,  1875 ; Pal.  Ohio,  vol. 

2,  p.  102,  pi.  4,  fig.  5.  (See  Aparchites  minutissima.) 

[ Leperditia  ( Isochilina )]  Ottawa  Jones,  1858;  Annals  Mag.  Nat.  Hist.,  London, 

3d  series,  vol.  1,  p.  248,  pi.  11,  fig.  1.  Chazy. 

[ Leperditia  ( Isochilina )]  Ottawa  Jones,  1858 ; Geol.  Survey  Canada,  decade  3,  p. 

97,  pi.  9,  fig.  14. 

Ottawa  Jones,  1884 ; Annals  Mag.  Nat.  Hist.,  London,  5th  series,  vol.  14,  p.  345. 

seelyi  (Whitfield)  Jones,  1890 ; Quait.  Jour.  Geol.  Soc.,  vol.  46,  p.  22,  pi.  1,  fig.  7. 

For  other  references,  see  Primitia  seelyi. 

Klcedenia  Jones  and  Holl,  1886;  Annals  Mag.  Nat.  Hist.,  London,  5th  series,  vol.  17, 
p.  362. 


V0GDES.] 


CATALOGUE  OF  NON-TRILOBITES. 


169 


Klcedenia  [Be-yrichia]  notata  Hall,  1859  ; Pal.  New  York,  vol.  3,  p.  379,  pi.  79  b,  figs. 
3 a,  b,  c.  Lower  Helderberg. 

[ Beyrichia ] notata  var.  ventricosa  Hall,  1859 ; idem,  p.  380,  pi.  79  b,  figs.  4 a,  b,  c. 

notata  Jones,  1890  ; Quart.  Jour.  Geol.  Soc.,  vol.  46,  p.  13,  pi.  4,  figs.  22,  23. 

notata  var.  ventricosa  Jones,  1890 ; Quart.  J6ur.  Geol.  Soc.,  vol.  46,  p.  14,  pi.  1, 

figs.  1 a,  b;  pi.  4,  fig.  24. 

pennsylvanica  Jones,  1889;  American  Geologist,  vol.  4,  p.  341,  pi.,  figs.  5-9. 

Lower  Helderberg. 

simplex  Jones,  1889 ; American  Geologist,  vol.  4,  p.  338,  pi.,  fig.  14. 

Upper  Devonian. 

Leaia  Jones,  1862 ; Mon.  Fossil  Estheriae,  p.  115. 

[ Cypricardia ] leidyi  Lea,  1855;  Proc.  Acad.  Nat.  Sci.  Phila.,  vol.  7,  p.  341,  pi.  4. 

Coal  Measures. 

leidyi  Jones,  1862;  Mon.  Fossil  Estheriae,  p.  116,  pi.  5,  figs.  11,  12. 

leidyi  Dawson,  1868 ; Acadian  Geology,  p.  256,  fig.  78  c. 

leidyi  Packard,  1882;  12th  Rept.  U.  S.  Geol.  Survey  Territories,  p.  358,  fig.  24. 

leidyi  Jones,  1870;  Geol.  Mag.,  vol.  7,  p.  219,  pi.  9,  fig.  11;  also,  Geol.  Mag., 

decade  3,  vol.  1,  p.  361,  pi.  12,  fig.  13. 

tricarinata  Meek  and  Worthen,  1868;  Geol.  Survey  Illinois,  vol.  3,  p.  541,  figs. 

Bi,  B2,  B:{.  Coal  Measures. 

tricarinata  White,  1884 ; 13th  Ann.  Rept.  Dept.  Geol.  Nat.  Hist.  Indiana,  p.  167, 

pi.  39,  figs.  10-13. 

Leperditia  Rouault,  1851 ; Bull.  Soc.  G6ol.  France,  2d  series,  vol.  8,  p.  377. 

[ Cytherina ] alta  Conrad,  1842;  Geol.  Rept.  New  York,  3d  Geol.  Dist.  (Vanuxem), 

p.  112.  Lower  Helderberg. 

[ Cytherina ] alta  ? Hall,  1852 ; Pal.  New  York,  vol.  2,  p.  338,  pi.  78,  figs.  2 a-d. 

Referred  to  Leperditia  jonesi  Hall,  idem,  vol.  3,  p.  372. 

alta  Jodos,  1856 ; Annals  and  Mag.  Nat.  Hist.,  London,  2d  series,  vol.  17,  p.  88,  pi. 

7,  figs.  6,  7. 

alta  Jones,  1858  ; Annals  Mag.  Nat.  Hist.,  London,  3d  series,  vol.  1,  p.  250,  pi.  10, 

figs.  10,  11. 

alta  Hall,  1859;  Pal.  New  York,  vol.  3,  p.  373,  pi.  79  a,  figs.  6 a-e. 

alta  Meek,  1873 ; Pal.  Ohio,  vol.  1,  p.  187,  pi.  17,  figs.  2 a,  b. 

alta  Jones,  1881';  Annals  Mag.  Nat.  Hist.,  London,  5th  series,  vol.  8,  p.  346. 

alta  Whitfield,  1882 ; Geol.  Wisconsin,  vol.  4,  p.  323,  pi.  25,  figs.  8, 9. 

alta  Jones,  1884 ; Annals  Mag.  Nat.  Hist.,  London,  5th  series,  vol.  14,  p.  343. 

alta  Jones,  1890 ; Quart.  Jour.  Geol.  Soc.,  vol.  46,  p.  25,  pi.  1,  figs.  6 a,  b. 

amygdalina  Jones,  1858;  Annals  Mag.  Nat.  Hist.,  London,  3d  series,  vol.  1,  p. 

341.  Trenton. 

amygdalina  Jones,  1858 ; Geol.  Survey  Canada,  decade  3,  p.  97,  pi.  11,  figs.  18, 19. 

amygdalina  Jones,  1881;  Annals  Mag.  Nat.  Hist.,  London,  5th  series,  vol.  8,  p. 

344,  pi.  19,  fig.  9. 

amygdalina  Jones,  1884 ; Annals  Mag.  Nat.  Hist.,  London,  5th  series,  vol.  14,  p. 

342. 

angulifera  Whitfield,  1881 ; Annals  New  York  Acad.  Sci.,  vol.  2,  p.  199. 

Lower  Helderberg. 

anna  Jones,  1858;  Annals  Mag.  Nat.  Hist.,  London,  3d  series,  vol.  1,  p.  347,  pi. 

9,  fig.  8.  Calciferous. 

anna  Jones,  1858;  Geol.  Survey  Canada,  decade  3,  p.  96,  pi.  11,  fig.  13. 

anticostiana  Jones,  1884  ; Annals  Mag.  Nat.  Hist.,  London,  3d  series,  vol.  14,  p. 

241.  Hudson. 

Syn.,  canadenns  var.  anticostiana  J ones,  1858;  Annals  Mag.  Nat.  Hist.,  London, 
3d  series,  vol.  1,  p.  341.  Hudson. 

canadensis  var.  anticostiana  Jones,  1858 ; Geol.  Survey  Canada,  decade  3,  p. 
95,  pi.  11,  fig.  17. 


170 


A BIBLIOGRAPHY  OF  PALEOZOIC  CRUSTACEA. 


[bull.  63. 


Leperditia  anticostiana  Billings,  1866;  Catalogue  Sil.  Foss.,  Anticosti,  p.  68. 

Syn.,  fabulUes  (Conrad)  var.  anticostiana  Jones,  1881;  Annals  Mag.  Nat.  Hist., 
London,  5th  series,  vol.  8,  p.  344,  pi.  19,  fig.  8. 

arctica  Jones,  1856;  Annals  Mag.  Nat.  Hist.,  London,  2d  series,  vol.  17,  p.  87, 

figs.  1-5.  Upper  Silurian. 

Syn.,  balthica  var.  arctica  (Jones)  Salter,  1852;  Appendix  Sutherland’s  Jour.  Voy- 
age Baffin's  Bay,  vol.  2,  p.  ccxxi,  pi.  5,  fig.  13. 
balthica  var.  arctica  (Jones)  Salter,  1853;  Quart.  Jour.  Geol.  Soc.  London, 
vol.  9,  p.  314. 

argenta  Walcott,  1886;  Bull.  U.  S.  Geol.  Survey,  No.  30,  p.  146,  pi.  8,  fig.  5. 

Middle  Cambrian. 

billingsi  Jones,  1856;  Annals  Mag.  Nat.  Hist.,  London,  2d  series,  vol.  8,  p.  345, 

pi.  15,  fig.  9.  Trenton. 

bivertex  Ulrich,  1879;  Jour.  Cincinnati  Soc.  Nat.  Hist.,  vol.  2,  p.  11,  pi.  7,  figs. 

5,5  a.  Hudson. 

bivia  White,  1874 ; Kept.  Invert.  Foss.  U.  S.  Geog.  and  Geol.  Survey  W.  100th 

Mer.,  p.  11.  Quebec. 

bivia  White,  1877;  U.  S.  Geog.  and  Geol.  Survey  W.  100th  Mer.,  Palseont.,  vol. 

4,  p.  58,  pi.  3,  figs.  7 a-d. 

byrnesi  Miller,  1874  ; Cincinnati  Quart.  Jour.  Sci.,  vol.  1,  p.  123,  fig.  10.  (See 

.SJchmina  beyrnesi.)  Hudson. 

caecigena  Miller,  1881;  Jour.  Cincinnati  Soc.  Nat.  Hist.,  vol.  1,  p.  263,  pi.  6, 

figs.  5,  5 a.  Hudson. 

canadensis  Jones,  1858;  Annals  Mag.  Nat.  Hist.,  London,  3d  series,  vol.  1,  p. 

244,  pi.  9,  figs.  ll-li>.  Chazy  and  Trenton. 

canadensis  Jones,  1858 ; Geol.  Survey  Canada,  decade  3,  p.  92 ; var.  nana,  pi.  11, 

figs.  6,7,9,10,  and  labrosa,  pi.  11,  fig.  8. 

canadensis  Jones,  1881 ; Annals  Mag.  Nat.  Hist.,  London,  5th  series,  vol.  14,  p. 

340. 

Compare  Leperditia  turgida,  L.  concinnula,  and  L.  ventralis. 

canadensis  var.  pauquettiana  Jones.  (See  Leperditia  louckana.) 

[Cy  there]  carbonaria  Hall,  1858;  Trans.  Albany  Inst.,  vol.  4,  p.  33.  Warsaw. 

carbonaria  Whitfield,  1882;  Bull.  Am.  Mus.  Nat.  Hist.,  New  York,  vol.  1,  p.  94, 

pi.  9,  figs.  24-27. 

capax  Safford ; Geol.  Tennessee.  (Not  defined. ) 

cayuga  Hall,  1861 ; Des.  New  Species  Foss.,  p.  83.  Corniferous. 

cayuga  Hall,  1862;  15th  Rept.  New  York  State  Cab.  Nat.  Hist.,  p.  111. 

claypolei  Jones,  1890;  Quart.  Jour.  Geol.  Soc.,  vol.  46,  p.  25,  pi.  3,  figs.  17  a-c. 

Cincinnati. 

concinnula  Billings,  1865;  Pal.  Fossils,  vol.  1,  p.  299.  Quebec. 

crepiformis  Ulrich,  1879;  Jour.  Cincinnati  Soc.  Nat.  Hist.,  vol.  2,  p.  10,  pi.  7, 

figs.  3, 3 a.  'Hudson. 

[ Cytherina ] cylindrica  Hall,  1852;  Pal.  N.  Y.,  vol.  2,  p.  14,  pi.  4,  figs.  8 a,  b. 

For  other  references,  see  Isochilina  cylindrica.  Medina. 

dermatoides  Walcott,  1887 ; Am.  Jour.  Sci.,  3d  series,  vol.  34,  p.  192,  pi.  1,  figs. 

13,  13  a.  Cambrian. 

faba  Hall,  1876;  28th  Rept.  New  York  State  Mus.  Nat.  Hist.,  Expl.,  pi.  32,  figs. 

1-3.  Niagara. 

faba  Hall,  1879;  28th  Rept.  New  York  State  Mus.  Nat.  Hist.,  p.  186,  pi.  32, 

figs.  1-3  (2d  ed.). 

faba  Hall,  1882;  11th  Aun.  Rept.  Dept.  Geol.  Nat.  Hist.  Indiana,  p.  331,  pi.  34, 

figs.  1-3, 

[ Cytherina ] fabulites  Conrad,  1843;  Proc.  Acad.  Nat.  Sci.  Phila.,  vol.  1,  p.  332. 

Trenton. 

fabulitea  Jones,  1856;  Annals  Mag.  Nat.  Hist.,  London,  2d  series,  vol.  17,  p.  89. 


CATALOGUE  OF  NON-TRILOB ITES. 


V0GDK8.J 


171 


Leperditia  fabulites  Jones,  1858  ; Annals  Mag.  Nat.  Hist.,  London,  3d  series,  vol.  1, 
p.  341. 

fabulites  Jones,  1881 ; Annals  Mag.  Nat.  Hist.,  London,  4th  series,  vol.  8,  p.  342. 

fabulites  Whitfield,  1883;  Geol.  Wisconsin,  vol.  1,  p.  60,  fig.  5. 

fabulites  Jones,  1884 ; Annals  Mag.  Nat.  Hist.,  London,  5th  series,  vol.  14,  p.  342. 

fonticola,  1867 ; 20th  Rept.  New  York  State  Cab.  Nat.  Hist.,  p.  335,  pi.  21,  figs. 

1-3.  Niagara. 

fonticola,  1870;  20th  Rept.  New  York  State  Cab.  Nat.  Hist.  (rev.  ed.),  p.  428, 

pi.  21,  figs.  1-3. 

gibbera  Jones,  1856;  Annals  Mag.  Nat.  Hist.,  London,  2d  series,  vol.  17,  p.  90, 

pi.  7,  figs.  1-3.  Niagara. 

gibbera  Jones,  1858;  Annals  Mag.  Nat.  Hist.,  London,  3d  series,  vol.  1,  p.  250, 

pi.  10,  figs.  7-9. 

gibbera  var.  scalaris  Jones,  1858;  Geol.  Survey  Penn.,  vol.  2,  p.  834,  fig.  698. 

gracilis.  (See  Isochilina  gracilis.) 

hudsonica  Hall,  1859 ; Pal.  New  York,  vol.  3,  p.  375,  pi.  79  a,  figs.  7 a,  b,  c. 

Lower  Helderberg. 

hudsonica  Jones,  1890  ; Quart.  Jour.  Geol.  Soc.,  vol.  46,  p.  24,  pi.  1,  figs.  5 a-c,  11 

a-c  ; pi.  3,  fig.  20  (?) 

jonesi  Hall,  1859 ; Pal.  New  York,  vol.  3,  p.  272,  pi.  79  a,  figs.  5 a-e. 

Lower  Helderberg. 

jonesi  Jones,  1884;  Annals  Mag.  Nat.  Hist.,  London,  5th  series,  vol.  1,  p.  343. 

Syn.,  alia  Hall,  1852 ; Pal.  New  York,  vol.  2,  p.  338,  pi.  78,  figs.  2 a-d. 

josephiana  Jones,  1884  ; Annals  Mag.  Nat.  Hist.,  London,  5th  series,  vol.  1,  p.  341. 

Trenton. 

Syn.,  canadensis  var.  josephiana  Jones,  1858;  Annals  Mag.  Nat.  Hist.,  London,  3d 
series,  vol.  1,  p.  341. 

canadensis  var.  josephiana  Jones,  1858  ; Geol.  Survey  Canada,  decade  3,  p.  94, 
pi.  11,  fig.  16. 

fabulites  var.  josephiana  Jones,  1881;  Annals  Mag.  Nat.  Hist.,  London,  5th 
series,  vol.  8,  p.  344,  pi.  19,  fig.  7 ; pi.  20,  figs.  7, 8;  also,  p.  345,  pi.  20,  fig.  4 (?). 
labrosa.  (See  Leperditia  canadensis. ) 

louckiana  Jones,  1884  ; Annals  Mag.  Nat.  Hist.,  London,  5th  series,  vol.  1,  p.  341. 

Trenton. 

Syn.,  canadensis  f Jones,  1858;  Annals  Mag.  Nat.  Hist., London, 3d  series,  vol.  1, 
p.  245,  pi.  9,  figs.  16, 17. 

Afterwards  var.  louckiana  and  Leperditia  canadensis  var . pauquettiana. 
canadensis  var.  louckiana  Jones,  1858;  Geol.  Survey  Canada,  decade  3,  p.  93, 
pi.  11,  fig.  11. 

fabulites  var.  louckiana  Jones,  1881;  Annals  Mag.  Nat.  Hist.,  London,  5th 
series,  vol.  8,  p.  343. 

[ Cypridina ] marginata  Keyserling,  1846;  Wiss.  Beob.  auf  einer  Reise  in  das 

Petochora-Land,  p.  288,  pi.  11,  fig.  16. 

marginata  Jones,  1858;  Annals  Mag.  Nat.  Hist.,  London,  3d  series,  vol.  17,  p. 

91,  pi.  7,  figs.  11, 14, 15. 

Syn.,  Cyridina  balthica  Eichwald  (not  Cytherina  balthica  Hisinger)  Bull.  Soc.  Nat. 
Moscou,  1854,  No.  1,  p.  99,  pi.  2,  fig.  6. 

[ Isochilina]  minutissima  Hall.  (Soe  Isochilina  minutissima. ) 

morgani  Safford;  Geol.  Tennessee.  (Not  defined.) 

Nana?  Jones,  1890;  Quart.  Jour.  Geol.  Soc.,  vol.  46,  p.  27,  pi.  4,  fig.  4.  (See, 

also,  Leperditia  canadensis  var.  nana.) 

okeni  (Munster)  Dawson,  1868;  Acadian  Geology,  p.  256,  fig.  78  b. 

Lower  Carboniferous. 

Ottawa.  (See  Isochilina  Ottawa.) 

ovata  Jones,  1858;  Annals  Mag.  Nat.  Hist.,  London,  3d  series,  vol.  1,  p.  252,  pi. 

10,  fig.  14.  Trenton 


172 


A BIBLIOGRAPHY  OF  PALEOZOIC  CRUSTACEA. 


|bull.63. 


Leperditia  ovata  Jones,  1858;  Geol.  Survey  Penn.,  vol.  2,  p.  834,  fig.  697. 

pauquettiana.  (See  Leperditia  canadensis  var.  pauquettiana. ) 

parasitica  Hall,  1859;  Pal.  New  York,  vol.  3,  p.  376,  pi.  79  a,  figs.  8 a,  b. 

Lower  Helderberg. 

Referred  by  T.  R.  Jones  to  Beyrichia  parasitica,  which  see. 

parvula  Hall,  1859 ; Pal.  New  York,  vol.  3,  p.  376,  pi.  79  a,  figs.  9 a,  b. 

Lower  Helderberg. 

pennsylvanica  Jones,  1858;  Annajs  Mag.  Nat.  Hist.,  London,  3d  series,  vol.  1,  p. 

251,  pi.  10,  figs.  12,  13.  Clinton. 

pennsylvanica  Jones,  1858 ; Geol.  Survey  Penn.,  vol.  2,  p.  834,  fig.  699. 

punctulifera  Hall,  1860;  13th  Rept.  New  York  State  Cab.  Nat.  Hist.,  p.  92.  (See 

Primitiopsis  punctulifera.)  Hamilton. 

radiata  Ulrich,  1879;  Jour.  Cincinnati  Soc.  Nat.  Hist.,  vol.  2,  p.  9,  pi.  7,  figs. 

2 a,  b.  Utica. 

rotundata  Walcott,  1884;  Pal.  Eureka  Dist.,  Mon.  U.  S.  Geol.  Survey,  vol.  8,  p. 

206,  pi.  16,  fig.  5.  Devonian. 

scalaris  (Leperditia  gibbera  var.  scalaris  Jones,  1858) ; Annals  Mag.  Nat.  Hist. 

London,  3d  series,  vol.  1,  p.  250,  pi.  10,  figs.  7-9.  Waterlime. 

seneca  Hall,  1861 ; Des.  New  Species  Fossils,  p.  84.  Hamilton. 

seneca  Hall,  1862;  15th  Rept.  New  York  State  Cab.  Nat.  Hist.,  p.  112. 

seneca  Jones,  1890;  Quart.  Jour.  Geol.  Soc.,  vol.  46,  p.  23,  pi.  1,  figs.  13,  14. 

sinuata  Hall,  1860 ; Canadian  Naturalist,  vol.  5,  p.  158.  Upper  Silurian. 

sinuata  Dawson,  1868;  Acadian  Geology,  p.  609,  fig.  217. 

sinuata  Jones,  1890;  Quart.  Jour.  Geol.  Soc.,  vol.  46,  p.  24,  pi.  1,  figs.  12  a-c. 

spinulifera  Hall,  186\,;  Des.  New  Species  Fossils,  p.  83.  Corniferous. 

spinulifera  Hall,  1862;  15th  Rept.  New  York  State  Cab.  Nat.  Hist.,  p.  111. 

[ Cythere ] sublaevis  Shumard,  1855;  1st  and  2d  Ann.  Rept.  Geol.  Survey  Mis- 
souri, p.  195,  pi.  B,  fig.  15.  Lower  Magnesian. 

subquadrata  Jones,  1889;  American  Geologist,  vol.  4,  p.  340,  pi.,  figs.  4 a-d. 

Lower  Helderberg. 

troyensis  Ford.  (See  Aristozoe  troyensis.) 

unicornis  Ulrich,  1879 ; Jour.  Cincinnati  Soc.  Nat.  Hist.,  vol.  2,  p.  10,  pi.  7,  figs. 

4,  4 a,  b.  Hudson. 

Referred  by  Prof.  T.  R.  Jones  to  Primitia  unicornis. 

ventralis  Billings,  1865;  Pal.  Fossils,  vol.  1,  p.  300.  Quebec. 

Lepidocoleus  Faber,  1886;  Jour.  Cincinnati  Soc.  Nat.  Hist.,  vol.  9,  p.  15. 

jamesi  (Hall  and  Whitfield)  Faber,  1886;  idem , vol.  9,  p.  15,  pi.  1,  figs.  a-f. 

Hudson. 

For  other  references,  see  Pumulites  jamesi. 

Lisgocaris  Clarke,  1882;  Am.  Jour.  Sci.,  3d  series,  vol.  23,  p.  478. 

lutheri  Clarke,  1882;  Am.  Jour.  Sci.,  3d  series,  vol.  23,  p.  478,  pi.  1,  fig.  5. 

Hamilton. 

Mesothyra  Hall,  1888 ; Pal.  New  York,  vol.  7,  p.  187. 

[ Dithyrocaris ] neptuni  Hall,  1876;  Illus.  Devonian  Fos.,  pi.  23  (not  pi.  22,  figs. 

1-5) ; pi.  23,  figs.  1-3.  Hamilton. 

[ Dithyrocaris ] neptuni  Packard,  1878 ; 12th  Rept.  U.  S.  Geol.  Survey  Territories, 

p.  452,  fig.  73. 

[ Dithyrocaris ] neptuni  Etheridge,  Woodward,  and  Jones,  1887 ; 5th  Rept.  Comm. 

Foss.  Phyllopoda  Pal.  Rocks,  p.  8. 

neptuni  Hall,  1888 ; Pal.  New  York,  vol.  7,  p.  191,  pi.  32,  fig.  7 ; pi.  33,  fig.  1. 

neptuni  Etheridge,  Woodward,  and  Jones,  1888 ; 6th  Rept.  Comm.  Foss.  Phyl- 
lopoda Pal.  Rocks,  p.  8. 

Syn.,  oceani  Hall,  1888;  Pal.  New  York,  vol.  7,  p.  187,  pi.  32,  figs.  1-6;  pi.  33,  fig. 
4-7;  pi.  34,  figs.  1-5.  Portage. 

[Dithyrocaris]  neptuni  Hall,  1876;  Illus.  Devonian  Foss.,  pi.  22,  figs.  1-5;  pi. 

33,  figs.  1-3. 


CATALOGUE  OF  NON-TRILOBITES. 


VOGDES.] 


173 


Mesothyra  IDithyrocaris ] neptuni  Etheridge,  Woodward,  and  Jones,  1887 ; 5th  Kept. 
Comm.  Foss.  Phyllopoda  Pal.  Rocks,  p.  8. 

Syn.,  Mesothyra  oceani  Etheridge,  Woodward,  and  Jones,  1888;  6th  Rept.  Comm. 
Foss.  Phyllopoda  Pal.  Rocks,  p.  8. 

atumea  Hall,  1888 ; Pal.  New  York,  vol.  7,  p.  193,  pi.  32,  figs.  8,  9 ; pi.  34,  fig.  2. 

Hamilton. 

atumea  Etheridge,  Woodward  and  Jones,  1888  ; 6th  Rept.  Comm.  Foss.  Phyllo- 
poda Pal.  Rocks,  p.  8. 

IDithyrocaris  ? ] veneris  Hall,  1888 ; Pal.  New  York,  vol.  7,  p.  193,  pi.  33,  fig.  3. 

Hamilton. 

IDithyrocaris  f J veneris  Etheridge,  Woodward,  and  Jones,  1888 ; 6th  Rept.  Comm. 

Foss.  Phyllopoda  Pal.  Rocks,  p.  8. 

Neolimulus  Woodward,  1868;  Geol.  Mag.,  vol.  5,  p.  1. 

Type,  Neolimulus  falcatus  Woodward. 

Nothozoe  Barrande,  1872;  Syst.  Sil.  Bohdme,  vol.  1,  suppl.,  p.  536. 

Type,  Nothozoe  pollens  Barrande. 

vermontana  Whitfield,  1884;  Bull.  Am.  Mus.  Nat.  Hist.,  vol.  1,  p.  144,  pi.  14, 

figs.  14,  15.  Potsdam. 

Falaeocaris  Meek  and  Worthen,  1865;  Proc.  Acad.  Nat.  Sci.  Phila.,  vol.  17,  p.  48. 

typus  Meek  and  Worthen,  1865;  Proc.  Acad.  Nat.  Sci.  Phila.,  vol.  17,  p.  49. 

Syn.,  Acanthotelson  incequalis  Meek  and  Worthen,  1865;  Proc.  Acad.  Nat.  Sci. 

Phila.,  vol.  17,  p.  48.  Coal  Measures. 

Acanthotelson  incequalis  Meek  and  Worthen,  1866 ; Geol.  Illinois,  vol.  2,  p.  403,  pi. 
32,  fig.  7,  7 a. 

typus,  Meek  and  Worthen,  1866;  Geol.  Illinois,  vol.  2,  p.  405,  pi.  32,  figs.  5 a-d. 

typus  Meek  and  Worthen,  1868^  Geol.  Illinois,  vol.  3,  p.  552,  iigs.  a,  b. 

typus  Peach,  1880 ; Trans.  Royal  Soc.  Edinburgh,  vol.  30,  p.  85,  pi.  10,  figs. 

10  g,  10  h. 

typus  Brocchi,  1880 ; Bull.  Soc.  G6ol.  France,  vol.  8,  p.  9,  pi.  1,  figs.  8-10. 

typus  Woodward,  1881 ; Geol.  Mag.,  decade  2,  vol.  8,  p.  533,  wood-cut. 

typus  White,  1884 ; 13th  Ann.  Rept.  Dept.  Geol.  Nat.  Hist.  Indiana,  p.  179,  pi. 

38,  figs.  1 2,  3. 

typus  Packard,  1885;  Am.  Naturalist,  vol.  19,  p.  790. 

typus  Packard,  1886;  Mem.  Nat.  Acad.  Sci.,  vol.  3,  p.  129,  pi.  3,  figs.  1-4  ; pi. 

7,  figs.  1,  2. 

Palceocrangon  Salter,  1861.  (See  Crangopsis  Salter,  1863.) 

Palaeopalaemon  Whitfield,  1880;  Am.  Jour.  Sci.,  3d  series,  vol.  19,  p.  40. 

newberryi  Whitfield,  1880;  Am.  Jour.  Sci.,  2d  series,  vol.  19,  p.  41.  Erie. 

newberryi  Whitfielcf,  1880  ; Author’s  Edition,  plate,  figs.  1,  2,  3. 

newberryi  Hall,  1888;  Pal.  New  York,  vol.  7,  p.  203,  pi.  30,  figs.  20-23. 

Palaeocreusia  Clarke,  1888 ; Pal.  New  York,  vol.  7,  p.  210. 

devonica  Clarke,  1888;  Pal.  New  York,  vol.  7,  p.  210,  pi.  36,  figs.  24,  26. 

Corniferous. 

Plumulites  Barrande,  1872;  Syst.  Sil.  Boh6me,  suppl.,  vol.  1,  p.  565. 

devonicus  Clarke,  1882;  Am.  Journ.  Sci.,  3d  series,  vol.  24,  p.  55,  figs.  1,  2. 

Hamilton. 

jamesi  Hall  and  Whitfield,  1875;  Pal.  Ohio,  vol.  2,  p.  106,  pi.  4,  figs.  1-3. 

Hudson. 

? jamesi  Miller,  1875  ; Cincinnati  Quart.  Jour.  Sci.,  vol.  2,  p.  275,  fig.  19. 

Referred  by  Faber  (Jour.  Cincinnati  Soc.  Nat.  Hist.,  vol.  9,  1886,  p.  15)  to  a 
new  genus  under  the  name  of  Lepidocoleus. 

newberryi  Whitfield,  1881 ; Annals  New  York  Acad.  Sci.,  vol.  2,  p.  217. 


Huron. 

Prestwichia  Woodward,  1867 ; Quart.  Jour.  Geol.  Soc.  London,  vol.  23,  p.  32. 


[BULL.  63. 


174  A BIBLIOGRAPHY  OF  PALEOZOIC  CRUSTACEA. 

Prestwichia  danse  (Meek  and  Wortken)  Packard,  1886;  Mem.  Nat.  Acad.  Sci.,  vol. 
3,  p.  146,  pi.  5,  figs.  3,  39 ; pi.  6,  figs.  1 a,  2,  2 a. 

For  other  references  to  this  species,  see  Euproops  and  Belinurua. 

eriensis  Williams.  (See  Protolimulus  eriensis.) 

Protolimulus  Packard,  1866;  Mem.  Nat.  Acad.  Sci.,  vol.  3,  p.  150. 

[Prestwichia ] eriensis  Williams,  1885  ; Am.  Jour.  Sci.,  3d  series,  vol.  30,  p.  45, 

3 figs.  Devonian. 

[Protolimulus')  eriensis  Packard,  1886;  Mem.  Nat.  Acad.  Sci.,  vol.  3,  p.  150, 

figs.  11-13. 

eriensis  Hall,  1888 ; Pal.  New  York,  vol.  7,  p.  153,  pi.  26,  figs.  1,  2. 

Primitia  Jones  and  Holl,  1865;  Annals  Mag.  Nat.  Hist.,  3d  series,  London,  vol.  16,  p. 
415. 

Primitia  cristata  Whitfield,  1889;  Bull.  Am.  Mus.  Nat.  Hist.,  New  York,  vol.  2,  p.  59, 
pi.  13,  figs.  1,  2.  (See  Isochilina  cristata.) 

gregaria  Whitfield,  1889;  Bull.  Am.  Mus.  Nat.  Hist.,  New  York,  vol.  2,  p.  58,  pi. 

13,  figs.  3-5.  (See  Isochilina  gregaria.) 

lativia  Ulrich, '1889 ; Contributions  Micro-Palaeont.,  pt.  2,  p.  50,  pi.  9,  figs.  8, 8 a. 

Hudson. 

[Beyrichia)  loganix ar.  leperditioides  Jones,  1858;  Annals  and  Mag.  Nat.  Hist., 

London,  3d  series,  vol.  1,  p.  244,  pi.  9,  fig.  10.  Trenton. 

[Beyrichia)  logani  var.  leperditoides  Jones,  1858;  Geol.  Survey  Canada,  decade 

3,  p.  91,  pi.  11,  figs.  1-5. 

leperditioides  Jones,  1884 : Annals  and  Mag.  Nat.  Hist.,  6th  series,  London, 

vol.  14,  p.  345. 

mundula  Jones,  1889;  American  Geologist,  vol.  4,  p.  337,  pi.,  figs.  1,2, 10, 15. 

Upper  Devonian. 

[Beyrichia  (Primitia))  occidentalis  Walcott,  1884 ; Pal.  Eureka  Diet.,  Mon.  U.  S. 

Geol.  Survey,  vol.  8,  p.  204,  pi.  17,  figs.  4,  4 a.  Devonian. 

[Beyrichia?)  parallels  Ulrich,  1889;  Contributions  Micro-PalaBont.,  pt.  2,  p.  51, 

pi.  9,  figs.  7-7  a.  Hudson. 

pennsylvanica  Jones,  1889 ; American  Geologist,  vol.  4,  p.  339,  pi.,  figs.  15  a,  b. 

Marcellus. 

seminulum  Jones,  1890;  Quart.  Jour.  Geol.  Soc.,  vol.  46,  p.  5,  pi.  2,  fig.  2. 

Hamilton. 

seelyi  Whitfield,  1889;  Bull.  Am.  Mus.  Nat.  Hist.,  N.  Y.,  vol.  2,  p.  60,  pi.  13,  figs. 

15-21.  (See  Isochilina  seelyi.) 

unicornis  (Ulrich)  Jones,  1890  ; Quart.  Jour.  Geol.  Soc.,  vol.  46,  p.  7,  pi.  11,  figs. 

8-13. 

For  other  references,  see  Beyrichia  unicornis  Ulrich.  The  species  is  referred 
by  Ulrich  (Contributions  Micro-Palseont.,  pt.  2,  p.  50)  to  Aparchites  unicornis, 
pi.  9,  fig.  11. 

whitfieldi  Jones,  1890;  Quart.  Jour.  Geol.  Soc.,  vol.  46,  p.  9,  pi.  3,  figs.  24  a,  b. 

Cincinnati. 

Primitiopsis  Jones,  1887 ; Notes  on  some  Sil.  Ostracoda  from  Gothland,  p.  5. 

punctulifera  (Hall)  Jones,  1890 ; Quart.  Jour.  Geol.  Soc.,  vol.  46,  p.  9,  pi.  2,  figs. 

7 a,  b,  12  a,  b.  * Hamilton. 

For  other  references,  see  Beyrichia  punctulifera  Hall. 

Protobalanus  Whitfield,  1889;  Bull.  Am.  Mus.  Nat.  Hist.,  New  York,  vol.  2,  p.  66; 
Hall,  1888;  Pal.  New  York,  vol.  7,  pp.  lxii  and  209. 

hamiltonensis  (Whitfield)  Hall,  1888 ; Pal.  New  York,  vol.  7,  p.  209,  pi.  36,  fig.  23. 

hamiltonensis  Whitfield,  1889 ; Bull.  Am.  Mus.  Nat.  Hist.,  New  York,  vol.  2,  p.  67, 

pi.  13,  fig.  22.  Marcellus. 

Protocaris  Walcott,  1884;  Bull.  U.  S.  Geol.  Survey,  No.  10,  p.  50. 

marshi  Walcott,  1884;  Bull.  U.  S.  Geol.  Survey,  No.  10,  p.  50,  pi.  10. 

Cambrian, 

• marshi  Walcott,  1886 ; Bull.  U.  S.  Geol.  Survey,  No.  30,  p.  148,  p\,  15,  fig.  1, 


V0GDE8.] 


CATALOGUE  OF  NON-TRI LOBITES. 


175 


Pterygotus  Agassiz,  1844 ; Mon.  Poissons  Fossiles,  note,  p.  xix. 

acuticauda  Pohlman,  1882 ; Ball.  Buffalo  Soc.  Nat.  Sci.,  vol.  4,  p.  42,  pi.  2, 

fig.  3.  Waterlime. 

bilobus  (Huxley  and  Salter)  Pohlman,  1886 ; Bull.  Buffalo  Soc.  Nat.  Sci.,  vol. 

5,  p.  27.  Waterlime. 

buffaloensis  Pohlman,  1881  ; Bull.  Buffalo  Soc.  Nat.  Sci.,  vol.  4,  p.  17,  figs.  1,2. 

Waterlime. 

buffaloensis  Pohlman,  1882 ; Bull.  Buffalo  Soc.  Nat.  Sci.,  vol.  4,  p.  44,  pi.  3, 

fig.  3. 

buffaloensis  Pohlman,  1886;  Bull.  Buffalo  Soc.  Nat.  Sci.,  vol.  5,  p.  24,  pi.  3,  fig.  1. 

canadensis  Dawson,  1881;  Canadian  Naturalist,  new  series,  vol.  9,  p.  103,  figs. 

1,2.  Niagara. 

cobbi  Hall,  1859;  Pal.,  New  York,  vol.  3,  p.  417,  pi.  83  b,  fig.  4;  pi.  84,  fig.  8 (?). 

Waterlime. 

cummingsi  Grote  and  Pitt,  1875;  Bull.  Buffalo  Soc.  Nat.  Sci., vol.  3,  p.  18,  figure. 

Waterlime. 

cummingsi  Grote  and  Pitt,  1878 ; Proc.  Am.  Assoc.  Adv.  Sci.,  26th  Meeting,  p. 

300,  figure. 

globicaudatus  Pohlman,  1882 ; Bull.  Buffalo  Soc.  Nat.  Sci.,  vol.  4,  p.  42,  pi.  2, 

fig.  2.  Waterlime. 

macrophthalmus  Hall,  1859;  Pal.  New  York,  vol.  3,  p.  418,  pi.  80  a,  figs.  8,8  a. 

Waterlime. 

macrophthalmus  Pohlman,  1882;  Bull.  Buffalo  Soc.  Nat.  Sci.,  vol.  4,  p.  44. 

osborni  Hall,  1859;  Pal.  New  York,  vol.  3,  p.  419,  pi.  80  a,  fig.  9.  Waterlime. 

quadricaudatus  Pohlman,  1882;  Bull.  Buffalo  Soc.  Nat.  Sci.,  vol.  4,  p.  43,  pi.  3, 

fig.  1.  Waterlime. 

Eachura  Scndder,  1878;  Proc.  Boston  Soc.  Nat.  Hist.,  vol.  19,  p.  296. 

Probably  the  same  as  the  genus  Dithyocaris. 

venom  Scudder,  1878;  Proc.  Boston  Soc.  Nat.  Hist.,  vol.  19,  p.  296. 

Coal  Measures. 

[ Dithyocaris  t ] venosa  Etheridge,  Woodward,  and  Jones,  1888;  6th  Kept.  Comm. 

Foss.  Phyllopoda,  p.  4. 

Rhinocaris  Clarke,  1888;  Pal.  New  York,  vol.  7,  p.  lviii. 

columbina  Clarke,  1888 ; Pal.  New  York,  vol.  7,  p.  195,  pi.  31,  figs.  16-21. 

Hamilton. 

columbina  Etheridge,  Woodward,  and  Jones,  1888 ; 6th  Rept.  Comm.  Foss.  Phyl- 
lopoda, etc.,  p.  8. 

acaphoptera  Hall,  1888;  Pal.  New  York,  vol.  7,  p.  197,  pi.  31,  figs.  22,  23. 

Hamilton. 

acaphoptera  Etheridge,  Woodward,  and  Jones,  1888;  6th  Rept.  Comm.  Foss. 

Phyllopoda  Pal.  Rocks,  p.  8. 

Schizodiscua  Clarke,  1888 ; Pal.  New  York,  vol.  7,  p.  207. 

capra  Clarke,  1888;  Pal.  New  York,  vol.  7,  p.  207,  pi.  25,  figs.  1-9.  Hamilton. 

SpathiocariB  Clarke,  1882;  Am.  Jour.  Sci.,  3d  series,  vol  23,  p.  477. 

emersoni  Clarke,  1882;  Am.  Jour.  Sci.,  3d  series, wol.  23,  p.  477,  pi.,  figs.  1-3. 

Hamilton. 

emersoni  Packard,  1883;  12th  Rept.  U.  S.  Geol.  Survey  Territories,  p.  451. 

emersoni  Clarke,  1886;  Neues  Jarbuch  fiir  Mineral.,  p.  180. 

emersoni  Woodward  and  Jones,  1884;  2d  Rept.  Comm.  Foss.  Phyllopoda  Pal. 

Rocks,  p.  7. 

emersoni  Clarke,  1885;  Bull.  U.  S.  Geol.  Survey,  No.  16,  p.  46. 

emersoni  Etheridge,  Woodward,  and  Jones,  1885 ; 3d  Rept.  Comm.  Foss.  Phyllo- 
poda Pal.  Rocks,  p.  3. 

emersoni  Ilall,  1888;  Pal.  New  York,  vol.  7,  p.  199,  pi.  35,  figs.  12-18. 

emersoni  Etheridge,  Woodward,  and  Jones,  1888;  6th  Rept.  Comm.  Foss.  Phyl- 
lopoda Pal.  Rocks,  p.  8, 


[BULL.  63. 


176  A BIBLIOGRAPHY  OF  PALEOZOIC  CRUSTACEA. 

Solenocaris  Meek,  1871;  Proc.  Acad.  Nat.  Sci.  Phila.,  vol.  23,  p.  335. 

The  name  Solenocaris  was  used  for  a species  of  fossil  Crustacea  by  Mr.  J.  Young 
in  1868.  Change  to  Strigocaris. 

ludovici  Worthen,  1884;  Bull.  Illinois  State  Cab.  Nat.  Hist.,  No.  2,  p.  3. 

St.  Louis. 

[Ceratiocaris  ( Solenocaris )]  strigata  Meek,  1872;  Proc.  Acad.  Nat.  Sci.  Phila.,  vol. 

23,  p.  335.  Waverly. 

[Ceratiocaris  ( Solenocaris )]  strigata  Meek,  1875;  Pal.  Ohio,  vol.  2,  p.  321,  pi.  18, 

figs.  4 a-c. 

Strigocaris,  name  suggested  to  replace  preoccupied  generic  name  Solenocaris  (Meek) 
Vogdes,  1889;  Annals  N.  Y.  Acad.  Sci.,  vol.  5,  p.  34. 

[Solenocaris]  st.  ludovici  Worthen,  1884;  Bull.  Illinois  State  Cab.  Nat.  Hist., 

No.  2,  p.  3.  St.  Louis. 

[Ceratiocaris  (Solenocaris)]  strigata  Meek,  1872;  Proc.  Nat.  Acad.  Sci.  Phila., 

vol.  23,  p.  335.  Waverly. 

[Ceratiocaris  ( Solenocaris )]  strigata  Meek,  1875;  Pal.  Ohio,  vol.  2,  p.  321,  pi.  18, 

figs.  4 a-c. 

Strobilepsis  Clarke,  1888 ; Pal.  New  York,  vol.  7,  p.  212. 

spinigera  Clarke,  1888 ; Pal.  New  York,  vol.  7,  p.  212,  pi.  36,  figs.  20-22. 

Hamilton. 

Stylonurus  Page,  1856;  Advance  Text-book  Geology. 

excelsior  Hall,  MSS.  Catskill. 

excelsior  Martin,  1882;  Trans.  New  York  Acad.  Sci.,  vol.  2,  p.  8. 

excelsior  Hall,  1884  ; 36th  Rept.  New  York  State  Mus.,  p.  77,  pi.  5,  fig.  1. 

excelsior  Hall,  1885 ; Proc.  Am.  Assoc.  Adv.  Sci.,  33d  Meeting,  p.  421. 

excelsior  Hall,  18£$3 ; Pal.  New  York,  vol.  7,  p.  156,  pi.  26 ; also  p.  221,  pi.  26  a. 

Compare  Dolichocephala  lacoana  Claypole. 

[Equistides]  wrightianus  Dawson,  1881 ; Quart.  Jour.  Geol.  Soc.,  vol.  37,  p.  303, 

pi.  12,  fig.  10;  pi.  13,  fig.  20.  Portage. 

[Equistides]  wrightianus  (Dawson)  Wright ; 35th  Rept.  New  York  State  Mus. 

Nat.  Hist.,  Expl.,  pi.  15,  note,  figs.  1,2. 

[Echinocaris]  wrightianus  Jones  and  Woodward,  1684;  Geol.  Mag.,  decade  3, 

vol.  1,  p.  3,  pi.  13,  figs.  1 a,  b. 

[Echinocaris]  wrightianus  Etheridge,  Woodward,  and  Jones,  1885 ; 3d  Rept. 

Comm.  Fossil  Phyllopoda  Pal.  Rocks,  p.  35. 

? [Echinocaris]  wrightianus  Hall,  1888;  Pal.  New  York,  vol.  7,  p.  160,  pi.  27, 

figs.  7-9. 

Strepula  Jones  and  Holl,  1886;  Annals  Mag.  Nat.  Hist.,  5th  series,  London,  vol.  17, 
p.  403. 

lunatifera  Ulrich,  1889;  Contributions  Micro-Palseont.,  pt.  2,  p.  56,  pi.  9,  tigs. 

14, 14  b.  Hudson. 

quadrilirata  (Hall  and  Whitfield)  Ulrich,  1889;  Contributions  Micro-Palseont., 

pt.  2,  p.  54,  pi.  9,  fig.  12. 

For  other  references,  see  Beyrichia  quadrilirata. 

sigmoidalis  Jones,  1890;  Quart.  Jour.  Geol.  Soc.,  vol.  46,  p.  11,  pi.  2,  fig.  4. 

Hamilton. 

Tropidocaris  Beecher,  1884  ; 2d  Geol.  Survey  Pennsylvania,  vol.  PPP,  p.  15. 

alternata  Beecher,  1884  ; 2d  Geol.  Survey  Penn.,  vol.  PPP,  p.  19,  pi.  2,  figs.  7, 8. 

Chemung. 

alternata  Etheridge,  Woodward,  and  Jones,  1885;  3d  Rept.  Comm.  Fobs.  Phyllo- 

poda  Pal.  Rocks,  p.  35. 

alternata  Hall,  1888;  Pal.  New  York,  vol.  7,  p.  186,  pi.  31,  figs.  14, 15. 

bicarinata  Beecher,  1884;  2d  Geol.  Survey  Penn.,  vol.  PPP,  p.  16,  pi.  2,  figs.  3-5. 

Chemung. 

bicarinata  Etheridge,  Woodward,  and  Jones,  1885;  3d  Rept.  Comm.  Foss.  Phyl- 
lopoda Pal.  Rocks,  p.  35. 


V0GDE6.] 


CATALOGUE  OF  NON-TRILOBITES. 


177 


Tropidocaris  bicarinata  Hall,  1888 ; Pal.  New  York,  vol.  7,  p.  184,  pi.  31,  figs.  7-12. 

Interrupta  Beecher,  1884;  2d  Geol.  Survey  Penn.,  vol.  PPP,  p.  18,  pi.  2,  fig.  5. 

Chemung. 

interrupta  Etheridge,  Woodward,  and  Jones,  1885  ; 3d  Kept.  Comm.  Foss. 

Phyllopoda  Pal.  Rocks,  p.  35. 

interrupta  Hall,  1888  ; Pal.  New  York,  vol.  7,  p.  185,  pi.  31,  figs.  7-12. 

Turrilepas  Woodward,  1865 ; Quart.  Jour.  Geol.  Soc.,  vol.  21,  p.  489. 

cancellatus  Hall,  1888 ; Pal.  New  York,  vol.  7,  p.  216,  pi.  36,  fig.  2. 

Corniferous. 

[ Plumulites]  devonicus  Clarke,  1882;  Am.  Jour.  Sci.,  3d  series,  vol.  24,  p.  55, 

figs.  1,2.  Hamilton. 

devonicus  Hall,  1888 ; Pal.  New  York,  vol.  7,  p.  215,  pi.  36,  fig.  1. 

flexuosus  Hall,  1888;  Pal.  New  York,  vol.  7,  p.  215,  pi.  36,  fig.  1.  Corniferous. 

foliatus  Hall,  1888;  Pal.  New  York,  vol.  7,  p.  218,  pi.  36,  fig.  15.  Hamilton. 

[ Plumulites ] newberryi  Whitfield,  1882 ; Annals  New  York  Acad.  Sci.,  vol.  2, 

p.  217.  Hamilton. 

newberryi  Hall,  1888;  Pal.  New  York,  vol.  7,  p.  219,  pi.  36,  figs.  16-19. 

nitidulus  Hall,  1888;  Pal.  New  York,  vol.  7,  p.  218,  pi.  36,  fig.  4.  Hamilton. 

squama  Hall,  1888 ; Pal.  New  York,  vol.  7,  p.  217,  pi.  36,  figs.  5-8.  Hamilton. 

tener  Hall,  1888 ; Pal.  New  York,  vol.  7,  p.  219,  pi.  36,  figs.  9-14.  Hamilton. 


Bull.  63 12 


© 


Title  for  subject  entry.  Author  title.  Series  title, 


LIBRARY  CATALOGUE  SLIPS. 

United  States.  Department  of  the  interior.  ( U.  S.  geological  survey ). 

Department  of  the  interior  [ — | Bulletin  | of  the  | United 
States  ! geological  survey  | no.  64  | [Seal  of  the  department]  | 

Washington  | government  printing  office  | 1890 

Second  title:  United  States  geological  survey  | J.  W.  Powell, 
director  | — | A report  of  work  done  | in  the  | division  of  chem- 
istry and  physics  | mainly  during  the  | fiscal  year  1888-’89  | — f 
F.  W.  Clarke,  chief  chemist  | [Vignette]  j 

Washington  | government  printing  office  | 1890 

8°.  60  pp. 


Clarke  (Frank  Wiggles  worth). 

United  States  geological  survey  | J.  W.  Powell,  director  | — | 
A report  of  work  done  | in  the  | division  of  chemistry  and  physics  | 
mainly  during  the  | fiscal  year  1888-89  | — | F.  W.  Clarke,  chief 
chemist  | [Vignette]  | 

Washington  | government  printing  office  | 1890 

8°.  60  pp. 

[United  States.  Department  of  the  interior.  (U.  S.  geological  survey). 

Bulletin  64]. 


United  States  geological  survey  | J.  W.  Powell,  director  | — | 
A report  of  work  done  | in  the  | division  of  chemistry  and  physics  | 
mainly  during  the  | fiscal  year  1888-89  | — | F.  W.  Clarke,  chief 
chemist  | [Vignette]  | 

Washington  | government  printing  office  | 1890 

8°.  60  pp. 

[United  States  Department  of  the  interior.  (77.  S.  geological  survey). 

Bulletin  64.] 


ADVERTISEMENT 


[Bulletin  No.  64.] 


The  publications  of  the  United  States  Geological  Survey  are  issued  in  accordance  with  the  statute 
approved  March  3,  1879,  which  declares  that— 

“ The  publications  of  the  Geological  Survey  shall  consist  of  the  annual  report  of  operations,  geological 
and  economic  maps  illustrating  the  resources  and  classification  of  the  lands,  and  reports  upon  general 
and  economic  geology  and  paleontology.  The  annual  report  of  operations  of  the  Geological  Survey 
shall  accompany  the  annual  report  of  the  Secretary  of  the  Interior.  All  special  memoirs  and  reports 
of  said  Survey  shall  be  issued  in  uniform  quarto  series  if  deemed  necessary  by  the  Director,  but  other- 
wise in  ordinary  octavos.  Three  thousand  copies  of  each  shall  be  published  for  scientific  exchanges 
and  for  sale  at  the  price  of  publication ; and  all  literary  and  cartographic  materials  received  ip  exchange 
shall  be  the  property  of  the  United  States  and  form  a part  of  the  library  of  the  organization : And  the 
money  resulting  from  the  sale  of  such  publications  shall  be  covered  into  the  Treasury  of  the  United 
States.” 

On  July  7,  1882,  the  folio  wing  .joint  resolution,  referring  to  all  Government  publications,  was  passed 
by  Congress: 

4 ‘ That  whenever  any  document  or  report  shall  be  ordered  printed  by  Congress,  there  shall  be  printed, 
in  addition  to  the  number  in  each  case  stated,  the  ‘ usual  number’  (1,900)  of  copies  for  binding  and 
distribution  among  those  entitled  to  receive  them.” 

Except  in  those  cases  in  which  an  extra  number  of  any  publication  has  been  supplied  to  the  Survey 
by  special  resolution  of  Congress  or  has  been  ordered  by  the  Secretary  of  the  Interior,  this  office  has 
no  copies  for  gratuitous  distribution. 

ANNUAL  REPORTS. 

I.  First  Annual  Report  of  the  United  States  Geological  Survey,  by  Clarence  King.  1880.  8°.  79  pp. 
1 map.— A preliminary  report  describing  plan  of  organization  and  publications. 

II.  Second  Annual  Report  of  the  United  States  Geological  Survey,  1880— '81,  by  J.  W.  Powell.  1882. 
8°.  lv,  588  pp.  61  pi.  1 map. 

III.  Third  Annual  Report  of  the  United  States  Geological  Survey,  1881-82,  by  J.  W.  Powell.  1883. 
8°.  xviii,  564  pp.  67  pi.  and  maps. 

IV.  Fourth  Annual  Report  of  the  United  States  Geological  Survey,  1882-83,  by  J.  W.  Powell.  1884. 
8°.  xxxii,  473  pp.  85  pi.  and  maps. 

V.  Fifth  Annual  Report  of  the  United  States  Geological  Survey,  1883-84,  by  J.  W.  Powell.  1885. 
8°.  xxxvi,  469  pp.  58  pi.  and  maps. 

VI.  Sixth  Annual  Report  of  the  United  States  Geological  Survey,  1884— ’85,  by  J.  W.  Powell.  1886. 
8°.  xxix,  570  pp.  65  pi.  and  maps. 

VII.  Seventh  Annual  Report  of  the  United  States  Geological  Survey,  1885-’86,  by  J.  W.  Powell.  1888. 
8°.  xx,  656  pp.  72  pi.  and  maps 

VIII.  Eighth  Annual  Report  of  the  United  States  Geological  Survey,  1886-87,  by  J.  W.  Powell.  1889. 
8°.  2 v.  xx,  1063  pp.  76  pi.  and  maps. 

IX.  Ninth  Annual  Report  of  the  United  States  Geological  Survey,  1887— ’88,  by  J.  W.  Powell.  1890. 
8°.  xiii,  717  pp.  88  pi.  and  maps. 

The  Tenth  Annual  Report  is  in  press. 

MONOGRAPHS. 

I.  Lake  Bonne  ville,  by  Grove  Karl  Gilbert.  1890.  4°.  xx,  438  pp.  51  pi.  1 map. 

II.  Tertiary  History  of  the  Grand  Canon  District,  with  atlas,  by  Clarence  E.  Dutton,  Capt.  U.  S.  A. 
1882.  4°.  xiv,  264  pp.  42  pi.  and  atlas  of  24  sheets  folio.  Price  $10.12. 

III.  Geology  of  the  Comstock  Lode  and  the  Washoe  District,  with  tlas,  by  George  F.  Becker.  1882. 
4°.  xv,  422  pp.  7 pi.  and  atlas  of  21  sheets  folio.  Price  $11.00. 

IV.  Comstock  Mining  and  Miners,  by  Eliot  Lord.  1883.  4°.  xiv,  451  pp.  3 pi.  Price  $1.50. 

V.  The  Copper-Bearing  Rocks  of  Lake  Superior,  by  Roland  Duer  Irving'  1883.  4°.  xvi,  464  pp. 
15  L 29  pi.  and  maps.  Price  $1.85. 


1 


II 


ADVERTISEMENT. 


VI.  Contributions  to  the  Knowledge  of  the  Older  Mesozoic  Flora  of  Virginia,  by  William  Morris 
Fontaine.  1883.  4°.  xi,  144  pp.  54 1.  54  pi.  Price  $1.05. 

VII.  Silver- Lead  Deposits  of  Eureka,  Nevada,  by  Joseph  Story  Curtis.  1884.  4°.  xiii,  200  pp.  16 
pi.  Price  $1.20. 

Vm.  Paleontology  of  the  Eureka  District,  by  Charles  Doolittle  Walcott.  1884.  4°.  xiii,  298  pp. 
241.  24  pi.  Price  $1.10. 

IX.  Brachiopoda  and  Lamellibranchiata  of  the  Raritan  Clays  and  Greensand  Marls  of  New  Jersey, 
by  Robert  P.  Whitfield.  1885.  4°.  xx,  338  pp.  35  pi.  1 map.  Price  $1.15. 

X.  Dinocerata.  A Monograph  of  an  Extinct  Order  of  Gigantic  Mammals,  by  Othniel  Charles  Marsh. 
1886.  4°.  xviii,  243  pp.  56 1.  56  pi.  Price  $2.70. 

XI.  Geological  History  of  Lake  Lahontan,  a Quaternary  Lake  of  Northwestern  Nevada,  by  Israel 
Cook  Russell.  1885.  4°.  xiv,  288  pp.  46  pi.  and  maps.  Price  $1.75. 

XII.  Geology  and  Mining  Industry  of  Leadville,  Colorado,  with  atlas,  by  Samuel  Franklin  Emmons. 
1886.  4°.  xxix,  770  pp.  45  pi.  and  atlas  of  35  sheets  folio.  Price  $8.40. 

XIII.  Geology  of  the  Quicksilver  Deposits  of  the  Pacific  Slope,  with  atlas,  by  George  F.  Becker. 
1888.  4°.  xix,  486  pp.  7 pi.  and  atlas  of  14  sheets  folio.  Price  $2.00. 

XIV.  Fossil  Fishes  and  Fossil  Plants  of  the  Triassic  Rocks  of  New  Jersey  and  the  Connecticut  Val- 
ley, by  John  S.  Newberry.  1888.  4°.  xiv,  152  pp.  26  pi.  Price  $1.00. 

XV.  The  Potomac  or  Younger  Mesozoic  Flora,  by  William  Morris  Fontaine.  1889.  4°.  xiv,  377 
pp.  180  pi.  Text  and  plates  bound  separately.  Price  $2.50. 

XVT.  The  Paleozoic  Fishes  of  North  America,  by  John  Strong  Newberry.  1889.  4°.  340  pp.  53  pi. 
Price  $1.00. 

In  preparation : 

— Description  of  New  Fossil  Plants  from  the  Dakota  Group,  by  Leo  Lesquereux. 

— Gasteropoda  of  the  New  Jersey  Cretaceous  and  Eocene  Marls,  by  R.  P.  Whitfield. 

— Geology  of  the  Eureka  Mining  District,  Nevada,  with  atlas,  by  Arnold  Hague. 

— Sauropoda,  by  O.  C.  Marsh. 

— Stegosauria,  by  O.  C.  Marsh. 

— Brontotheridae,  by  O.  C.  Marsh. 

— The  Penokee  Iron-Bearing  Series  of  Northern  Wisconsin  and  Michigan,  by  Roland  D.  Irving  and 
C.  R.  Van  Hise. 

— Report  on  the  Denver  Coal  Basin,  by  S.  F.  Emmons. 

— Report  on  Silver  Cliff  and  Ten-Mile  Mining  Districts,  Colorado,  by  S.  F.  Emmons. 

— Flora  of  the  Dakota  Group,  by  J.  S.  Newberry. 

— The  Glacial  Lake  Agassiz,  by  Warron  Upham. 

— Geology  of  the  Potomac  Formation  in  Virginia,  by  W.  M.  Fontaine. 

BULLETINS. 

1.  On  Hypersthene-Andesite  and  on  Triclinic  Pyroxene  in  Augitic  Rocks,  by  Whitman  Cross,  with  a 
Geological  Sketch  of  Buffalo  Peaks,  Colorado,  by  S.  F.  Emmons.  1883.  8°.  42  pp.  2 pi.  Price  10  cents. 

2.  Gold  and  Silver  Conversion  Tables,  giving  the  coining  values  of  troy  ounces  of  fine  metal,  etc.,  com- 
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3.  On  the  Fossil  Faunas  of  the  Upper  Devonian,  along  the  meridian  of  76°  30',  from  Tompkins  County, 
N.  Y.,  to  Bradford  County,  Pa.,  by  Henry  S.  Williams.  1884.  8°.  36  pp.  Price  5 cents. 

4.  On  Mesozoic  Fossils,  by  Charles  A.  White.  1884.  8°.  36  pp.  9 pi.  Price  5 cents. 

5.  A Dictionary  of  Altitudes  in  the  United  States,  compiled  by  Henry  Gannett.  1884.  8°.  325  pp. 
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7.  Mapoteca  Geologica  Americana.  A Catalogue  of  Geological  Maps  of  America  (North  and  South), 
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8°.  184  pp.  Price  10  cents. 

8.  On  Secondary  Enlargements  of  Mineral  Fragments  in  Certain  Rocks,  by  R.  D.  Irving  and  C.  R. 
Van  Hise.  1884.  8°.  56  pp.  6 pi.  Price  10  cents. 

9.  AReport  of  work  done  in  the  Washington  Laboratory  during  the  fiscal  year  1883-’84.  F.  W . Clarke, 
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10.  On  the  Cambrian  Faunas  of  North  America.  Preliminary  studies,  by  Charles  Doolittle  Walcott. 
1884.  8°.  74  pp.  10  pi.  Price  5 cents. 

11.  On  the  Quaternary  and  Recent  Mollusca  of  the  Great  Basin ; with  Descriptions  of  New  Forms,  by 
R.  Ellsworth  Call.  Introduced  by  a sketch  of  the  Quaternary  Lakes  of  the  Great  Basin,  by  G.  • K. 
Gilbert.  1884.  8°.  66  pp.  6 pi.  Price  5 cents. 

12.  A Crystallographic  Study  of  the  Thinolite  of  Lake  Lahontan,  by  Edward  S.  Dana.  1884.  8°. 
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13.  Boundaries  of  the  United  States  and  of  the  several  States  and  Territories,  with  a Historical 
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14.  The  Electrical  and  Magnetic  Properties  of  the  Iron-Carburets,  by  Carl  Barus  and  Vincent 
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ADVERTISEMENT. 


Ill 


15.  On  the  Mesozoic  and  Cenozoic  Paleontology  of  California,  by  Charles  A.  White.  1885.  8°. 
33  pp.  Price  5 cents. 

16.  On  the  Higher  Devonian  Faunas  of  Ontario  County,  New  York,  by  JohnM.  Clarke.  1885.  8°. 
86  pp.  3 pi.  Price  5 cents. 

17.  On  the  Development  of  Crystallization  in  the  Igneous  Rocks  of  Washoe,  Nevada,  with  Notes  on 
the  Geology  of  t he  District,  by  Arnold  Hague  and  Joseph  P.  Iddings.  1885.  8°.  44  pp.  Price  5 cents. 

18.  On  Marine  Eocene,  Fresh- water  Miocene,  and  other  Fossil  Mollusca  of  Western  North  America, 
by  Charles  A.  White.  1885.  8°.  26  pp.  3 pi.  Price  5 cents. 

19.  Notes  on  the  Stratigraphy  of  California,  by  George  F.  Becker.  1885.  8°.  28  pp.  Price  5 cents. 

20.  Contributions  to  the  Mineralogy  of  the  Rocky  Mountains,  by  Whitman  Cross  and  W.  F.  Hille- 
brana.  1885.  8°.  114  pp.  1 pi.  Price  10  cents. 

21.  The  Lignites  of  the  Great  Sioux  Reservation.  A Report  on  the  Region  between  the  Grand  and  Mo- 
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22.  On  New  Cretaceous  Fossils  from  California,  by  Charles  A.  White.  1885.  8°.  25  pp.  5 pi.  Price 

5 cents. 

23.  Observations  on  the  Junction  between  the  Eastern  Sandstone  and  the  Keweenaw  Series  on 

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24.  List  of  Marine  Mollusca,  comprising  the  Quaternary  Fossils  and  recent  forms  from  American 
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1885.  8°.  336  pp.  Price  25  cents. 

25.  The  Present  Technical  Condition  of  the  Steel  Industry  of  the  United  States,  by  Phineas  Barnes. 
1885.  8°.  85  pp.  Price  10  cents. 

26.  Copper  Smelting,  by  Henry  M.  Howe.  1885.  8°.  107  pp.  Price  10  cents. 

27.  Report  of  work  done  in  the  Division  of  Chemistry  and  Physics,  mainly  during  the  fiscal  year 

1884- ’85.  1886.  8°.  80  pp.  Price  10  cents. 

28.  The  Gabbros  and  Associated  Hornblende  Rocks  occurring  in  the  Neighborhood  of  Baltimore,  Md., 
by  George  Huntington  Williams.  1886.  8°.  78  pp.  4 pi.  Price  10  cents. 

29.  On  the  Fresh- water  Invertebrates  of  the  North  American  Jurassic,  by  Charles  A.  White.  1886. 

8°.  41  pp.  4 pi.  Price  5 cents. 

30.  Second  Contribution  to  the  Studies  on  the  Cambrian  Faunas  of  North  America,  by  Charles  Doo- 
ittle  Walcott.  1886.  8°.  369  pp.  33  pi.  Price  25  cents. 

31.  Systematic  Review  of  our  Present  Knowledge  of  Fossil  Insects,  including  Myriapods  and  Arach- 
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32.  Lists  and  Analyses  of  the  Mineral  Springs  of  the  United  States;  a Preliminary  Study,  by  Albert 
C.  Peale.  1886.  8°.  235  pp.  Price  20  cents. 

33.  Notes  on  the  Geology  of  Northern  California,  by  J.  S.  Diller.  1886.  8°.  23  pp.  Price  5 cents. 

34.  On  the  relation  of  the  Laramie  Molluscan  Fauna  to  that  of  the  succeeding  Fresh- water  Eocene 
and  other  groups,  by  Charles  A.  White.  1886.  8°.  54  pp.  5 pi.  Price  10  cents. 

35.  Physical  Properties  of  the  Iron-Carburets,  by  Carl  Barus  and  Vincent  Strouhal.  1886.  8°.  62 
pp.  Price  10  cents. 

36.  Subsidence  of  Fine  Solid  Particles  in  Liquids,  by  Carl  Barus.  1886.  8°.  58  pp.  Price  10  cents. 

37.  Types  of  the  Laramie  Flora,  by  Lester  F.  Ward.  1887.  8°.  354  pp.  57  pi.  Price  25  cents. 

38.  Peridotite  of  Elliott  County,  Kentucky,  by  J.  S.  Diller.  1887.  8°.  31  pp.  1 pi.  Price  5 cents. 

39.  The  Upper  Beaches  and  Deltas  of  the  Glacial  Lake  Agassiz,  by  Warren  Uphara.  1887.  8°.  84 

pp.  1 pi.  Price  10  cents. 

40.  Changes  in  River  Courses  in  Washington  Territory  due  to  Glaciation,  by  Bailey  Willis.  1887.  8°. 
10  pp.  4 pi.  Price  5 cents. 

41.  On  the  Fossil  Faunas  of  the  Upper  Devonian — the  Genesee  Section,  New  York,  by  Henry  S. 
Williams.  1887.  8°.  121  pp.  4 pi.  Price  15  cents. 

42.  Report  of  work  done  in  the  Division  of  Chemistry  and  Physics,  mainly  during  the  fiscal  year 

1885- 86.  F.  W.  Clarke,  chief  chemist.  1887.  8°.  152  pp.  1 pi.  Price  15  cents. 

43.  Tertiary  and  Cretaceous  Strata  of  the  Tuscaloosa,  Tombigbee,  and  Alabama  Rivers,  by  Eugene 
A.  Smith  and  Lawrence  C.  Johnson.  1887.  8°.  189  pp.  21  pi.  Price  15  cents. 

44.  Bibliography  of  North  American  Geology  for  1886,  by  Nelson  H.  Darton.  1887.  8°.  35  pp. 
Price  5 cents. 

45.  The  Present  Condition  of  Knowledge  of  the  Geology  of  Texas,  by  Robert  T.  Hill.  1887.  8°.  94 

pp.  Price  10  cents. 

46.  Nature  and  Origin  of  Deposits  of  Phosphate  of  Lime,  by  R.  A.  F.  Penrose,  jr.,  with  an  Introduc- 
tion by  N.  S.  Shale  r.  1888.  8°.  143  pp.  Price  15  cents. 

47.  Analyses  of  Waters  of  the  Yellowstone  National  Park,  with  an  Account  of  the  Methods  of  Anal- 
ysis employed,  by  Frank  Austin  Gooch  and  James  Edward  Whitfield.  1888.  8°.  84  pp.  Price  10 

cents. 

48.  On  the  Form  and  Position  of  the  Sea  Level,  by  Robert  Simpson  Woodward.  1888.  8°.  88  pp. 

Price  10  cents. 

49.  Latitudes  and  Longitudes  of  Certain  Points  in  Missouri,  Kansas,  and  New  Mexico,  by  Robert 
Simpson  Woodward.  1889.  8°.  133  pp.  Price  15  cents. 


IV 


ADVERTISEMENT. 


50.  Formulas  and  Tables  to  facilitate  the  Construction  and  Use  of  Maps,  by  Robert  Simpson  Wood- 
ward. 1889.  8°.  124  pp.  Price  15  cents. 

51.  On  Invertebrate  Fossils  from  the  Pacific  Coast,  by  Charles  Abiathar  White.  1889.  8°.  102  pp. 
14  pi.  Price  15  cents. 

52.  Subaerial  Decay  of  Rocks  and  Origin  of  the  Red  Color  of  Certain  Formations,  by  Israel  Cook 
Russell.  1889.  8°.  65  pp.  5 pi.  Price  10  cents. 

53.  The  Geology  of  Nantucket,  by  Nathaniel  Southgate  Shaler.  1889.  8°.  55  pp.  10  pi.  Price  10 
cents. 

54.  On  the  Thermo-Electric  Measurement  of  High  Temperatures,  by  Carl  Barus.  1889.  8°.  313  pp. 
incl.  1 pi.  11  pi.  Price  25  cents. 

55.  Report  of  work  done  in  the  Division  of  Chemistry  and  Physics,  mainly  during  the  fiscal  year 

1886- 87.  Frank  Wigglesworth  Clarke,  chief  chemist.  1889.  8°.  96  pp.  Price  10  cents. 

56.  Fossil  Wood  and  Lignite  of  the  Potomac  Formation,  by  Frank  Hall  Knowlton.  1889.  8°.  72  pp. 
7 pi.  Price  10  cents. 

57.  A Geological  Reconnaissance  in  Southwestern  Kansas,  by  Robert  Hay.  1890.  8°.  49  pp.  2 pi. 
Price  5 cents. 

59.  The  Gabbros  and  Associated  Rocks  in  Delaware,  by  Frederick  D.  Chester.  1890.  8°.  45  pp. 

1 pi.  Price  10  cents. 

60.  Report  of  work  done  in  the  Division  of  Chemistry  and  Physics,  mainly  during  the  fiscal  year 

1887- 88.  F.  W.  Clarke,  chief  chemist.  1890.  8°.  174  pp.  Price  15  cents. 

61.  Contributions  to  the  Mineralogy  of  the  Pacific  Coast,  by  William  Harlow  Melville  and  Waldemar 
Lindgren.  1890.  8°.  40  pp.  Price  5 cents. 

64.  A Report  of  work  done  in  the  Division  of  Chemistry  and  Physics,  mainly  during  the  fiscal  year 

1888- 89.  F.  W.  Clarke,  chief  chemist.  1890.  8°.  60  pp.  Price  10  cents. 

In  press: 

58.  The  Glacial  Boundary  in  Western  Pennsylvania,  Ohio,  Kentucky,  Indiana,  and  Illinois,  by  George 
Frederick  Wright. 

62.  The  Greenstone  Schist  Areas  of  the  Menominee  and  Marquette  Regions  of  Michigan,  by  George 
H.  Williams;  with  an  Introduction  by  R.  D.  Irving. 

63.  A Bibliography  of  Paleozoic  Crustacea  from  1698  to  1889,  including  a list  of  North  American 
species  and  a systematic  arrangement  of  genera,  by  A.  W.  Vogdes. 

65.  Comparative  Stratigraphy  of  the  Bituminous  Coal  Rocks  of  the  Northern  Half  of  the  Appala- 
chian Field,  by  I.  C.  White. 

66.  On  a Group  of  Volcanic  Rocks  from  the  Tewan  Mountains,  New  Mexico,  and  on  the  occurrence 
of  Primary  Quartz  in  certain  Basalts,  by  J.  P.  Iddings. 

In  preparation : 

— Natural  Gas  Districts  in  Indiana,  by  Arthur  John  Phinney. 

— On  the  relations  of  the  Traps  of  the  Jura-Trias  of  New  Jersey,  by  N.  H.  Darton. 

— The  Viscosity  of  Solids,  by  Carl  Barus. 

— Mesozoic  Fossils  in  the  Permian  of  Texas,  by  C.  A.  White. 

— A Late  Volcanic  Eruption  in  Northern  California  and  its  Peculiar  Lava,  by  J.  S.  Diller. 

— Altitudes  between  Lake  Superior  and  the  Rocky  Mountains,  by  Warren  Upham. 

STATISTICAL  PAPERS. 

Mineral  Resources  of  the  United  States,  1882,  by  Albert  Williams,  jr.  1883.  8°.  xvii,  813  pp.  Price 
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Mineral  Resources  of  the  United  States,  1883  and  1884,  by  Albert  Williams,  jr.  1885.  8°.  xiv,  1916 
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Mineral  Resources  of  the  United  States,  1888,  by  David  T.  Day.  1890.  8°. 

The  money  received  from  the  sale  of  these  publications  is  deposited  in  the  Treasury,  and  the  Secre- 
tary of  that  Department  declines  to  receive  bank  checks,  drafts,  or  postage  stamps ; all  remittances, 
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the  Survey  should  be  addressed 

To  the  Director  of  the 

United  States  Geological  Survey, 

Washington,  D.  C. 

Washington,  D.  C.,  June , 1890. 


DEPARTMENT  OF  THE  INTERIOR 


BULLETIN 

OF  THE 


UNITED  STATES 

GEOLOGICAL  SURVEY 


3STo.  64 


WASHINGTON 
GOVERNMENT  PRINTING  OFFICE 
1890 


UNITED  STATES  GEOLOGICAL  SURVEY 

J.  W.  POWELL,  DIRECTOR 


A REPORT  OF  WORK  DONE 

# 

IN  THE 

DIVISION  OF  CHEMISTRY  AND  PHYSICS 

MAINLY  DURING  THE 

FIS  CAL  YEAR  1888-’89 


WASHINGTON 

GOVERNMENT  PRINTING  OFFICE 
1890 


CONTENTS 


Page. 

Preface 7 

A theory  of  the  mica  group.  By  F.  W.  Clarke 9 

A platiniferous  nickel  ore  from  Canada.  By  F.  W.  Clarke  and  Charles  Catlett.  20 

A new  occurrence  of  gyrolite.  By  F.  W.  Clarke 22 

Analyses  of  three  descloizites  from  new  localities.  By  W.  F.  Hillebrand 24 

A new  meteorite  from  Mexico.  By  J.  E.  Whitfield 29 

Dumortierite  from  Harlem,  N.  Y.,  and  Clip,  Ariz.  By  J.  S.  Diller  and  J.  E. 

Whitfield 31 

Chemical  action  between  solids.  By  William  Hallock 34 

The  flow  of  solids;  a note.  By  William  Hallock 38 

Miscellaneous  analyses 40 

5 


i 


PREFACE. 


The  present  bulletin  represents  work  finished  in  the  Division  of 
Chemistry  and  Physics  during  the  fiscal  year  1888-’89,  and  resembles 
in  general  design  and  purpose  its  predecessors,  Nos.  9,  27,  42,  55,  and 
60.  It  covers,  however,  only  a part  of  the  work  actually  accomplished, 
for  some  investigations  are  not  yet  completed,  others  will  appear  in 
special  bulletins  now  in  course  of  preparation,  and  many  analyses  will 
be  published  in  forthcoming  reports  of  the  field  geologists. 

F.  W.  Clarke, 

Chief  Chemist 


WORK  DONE  IN  THE  DIVISION  OF  CHEMISTRY  AND 
PHYSICS  IN  1888-89. 


A THEORY  OF  THE  MICA  GROUP. 


By  F.  W.  Clarke. 


Ever  since  its  publication  in  1878, 1 in  spite  of  a few  dissentient 
voices,  Tschermak’s  theory  of  the  mica  group  has  been  generally  in 
vogue.  Nevertheless,  upon  careful  inspection,  the  theory  seems  open 
to  serious  objections.  In  brief,  omitting  details  for  the  present, 
Tschermak  regards  the  micas  as  made  up  of  four  fundamental  mole-  • 
cules;  to  which  the  following  formulae  are  assigned: 

1.  R'6Al6Si6024. 

2.  Mg14Si6024. 

3.  HgSiioO^. 

4.  F24Siio08. 

B'  stands  obviously  for  K,  Na,  Li,  or  H ; Mg  is  equivalent  to  Fe",  and 
aluminum  may  be  replaced  by  ferric  iron.  The  first  of  these  formulae 
represents  fairly  well  the  composition  of  normal  muscovite  and  para- 
gonite ; the  only  objection  to  it  being  that,  as  used  by  Tschermak,  it  as- 
sumes the  double  atom  of  quadrivalent  aluminum.  Since  it  has  been 
proved  by  Nilson  and  Petterson,  Combes,  Quincke,  and  others,  that 
aluminum  is  truly  trivalent,  the  formula  should  become  B^A^S^O^; 
which,  as  I have  shown  in  several  previous  papers,  may  be  regarded  as 
a substitution  derivative  of  normal  aluminum  orthosilicate. 

The  second,  third,  and  fourth  of  Tschermak’s  formulae  represent 
hypothetical  compounds,  the  second  being  a polymer  of  chrysolite,  to 
which,  in  nature,  some  varieties  of  talc  offer  the  nearest  approximation. 
The  third  and  fourth  formulae  are  analogous  to  no  known  substances, 
and  are,  moreover,  improbable  chemically.  No  mica,  by  itself,  resembles 
in  composition  either  of  the  three.  One  formula,  then,  corresponds  to 
an  observed  mineral,  while  the  others  are  purely  speculative ; a state 
of  affairs  which  is  not  altogether  satisfactory.  Furthermore,  the  four 
formulae  represent  as  many  distinct  chemical  types,  whereas  it  would 
seem  as  if  all  the  true  micas  should  be  reducible  to  one  general  form, 
under  which  their  isomorphism  would  be  more  readily  intelligible. 

lBer.  Wien.  Akad.,  vol.  78,  p.  5.  Zeitschr.  Kryst.,  vol.  3,  p.  122. 

9 


10 


WASHINGTON  LABORATORY. 


[BULL.  64. 


There  is  still  another  objection  to  Tschermak’s  system  of  formulae, 
which,  if  sustained  by  future  investigation,  will  be  fatal.  XJnder  his 
theory  the  ratio  of  oxygen  to  silicon  in  the  micas  can  never  exceed  four 
to  one;  while  the  published  analyses  of  micas  often  show  values  far 
higher,  ranging  in  some  cases  nearly  up  to  five.  In  certain  instances, 
as  Tschermak  himself  suggests,  this  excess  of  oxygen  over  the  ortho* 
silicate  ratio  may  be  due  to  water  inclosed  between  micaceous  laminae; 
and  in  other  cases  it  may  indicate  partial  alteration.  There  are  micas, 
however,  in  which  neither  of  these  explanations  appears  to  be  satisfac- 
tory, and  the  weight  of  evidence  goes  to  show  that  the  excess  of 
oxygen  is  essential.  If  this  be  true,  Tschermak’s  theory  is  so  far  inade- 
quate, for  to  such  micas  it  can  not  apply  without  serious  modification. 
The  question  can  only  be  settled  experimentally,  but  at  present  the 
objection  raised  by  it  can  not  be  ignored.  Some  of  its  details  will  be 
considered  later. 

jSTow,  in  order  to  conclusively  replace  Tschermak’s  theory  by  some- 
thing better,  two  fundamental  conditions  must  be  satisfied.  First,  all 
micas,  with  the  possible  exception  of  the  pseudomica,  margarite,  should 
be  reducible  to  one  general  type  of  formula,  which  shall  express  all 
known  relations  equally  well  with  the  formulae  proposed  by  Tschermak. 
Secondly,  hypothetical  compounds  must  be  so  far  as  possible  avoided, 
and  admitted  into  consideration  only  when  their  assumption  can  be 
shown  to  be  absolutely  necessary.  The  chief  difficulties  to  be  over- 
come are  the  variations  in  the  silicon -oxygen  ratio,  and  the  presence  of 
fluorine  in  many  common  micas. 

In  a number  of  papers  published  during  the  past  four  years,1 1 have 
sought  to  show  that  all  orthosilicates  containing  aluminum  may  be 
represented  as  substitution  derivatives  of  the  normal  salt  Al4(Si04)3. 
Muscovite  can  be  so  derived,  theoretically,  through  the  replacement  of 
one  aluminum  atom  by  R'3;  and  in  many  other  cases  we  have  equal 
simplicity  of  expression.  The  ferro- magnesian  micas,  the  phlogopites, 
and  the  lepidolites,  however,  are  less  simply  derived;  and  I have  in 
certain  cases  suggested  a linking  together  of  two  orthosilicate  nuclei 
to  the  group  Al2(Si04)5  in  order  to  account  for  their  formation.  I am 
now  inclined  to  believe,  however,  that  all  the  true  micas  are  referable 
to  the  same  general  type,  and  have  discussed  nearly  one  hundred 
published  analyses  from  that  point  of  view.  If  we  take  magnesium  as 
a generic  representative  of  the  bivalent  metals,  and  give  univalent 
elements  or  groups  the  general  symbol  R,  we  can  imagine  the  following 
derivatives  of  Al4(Si04)3  as  easily  possible: 


l. 

Si04  E R: 
Al  — Si04 
\i04  ~A1 


Al 


2. 

Si04  E Rs 

Al  — Si04=R3 

\ 

Si04  E Al 


3. 

Si04  — R3 

/ 

Al  — Si04  = R3 

\ 

Si04  — R3 


' Am.  Jour.  Sci.,  Nov.,  1886,  and  Aug.,  1887.  Also,  Am.  Cbem.  Jour.,  vol.  10,  p.  120 
(March,  1888). 


CLARKE.] 


A THEORY  OF  THE  MICA  GROUP. 


11 


Al  — Si04EAl 


Si04  = MgR 


4. 


5. 

Si04  EE  MgR 
Al  — Si04=MgR 
Si04  EE  Al 


To  these  we  may  add,  as  No.  7,  the  compound  Al2(Si04)6Mg9,  the  biv- 
alent analogue  of  No.  3,  and  identical  in  type  with  it.  Now,  so  long  as 
we  have  only  orthosilicate  micas  to  consider,  these  seven  formulae  cover 
all  their  variations  in  composition ; provided  that  fluorine,  when  pres- 
ent, is  represented  either  by  — Mg— F or  -A1=F2,  univalent  groups 
which  are  included  under  the  general  symbol  IF.  Most  of  the  micas 
appear  as  intermediate  mixtures  of  these  presumably  isomorphous  types. 
No.  1 represents  muscovite  and  paragonite,  and  No.  6 agrees  tolerably 
with  some  phlogopites.  No.  2 may  be  resolved  into  a mixture,  in  equal 
molecules,  of  No.  1 and  3 ; and  similarly  No.  5 may  be  regarded  as  com- 
posed of  Nos.  4 and  6.  Nos.  5 and  6,  moreover,  may  be  simplified  into 
mixtures  between  3 and  7,  so  that  numbers  1,  3,  4,  and  7 represent  all 
the  necessary  relations.  Even  No.  4 is  possibly  superfluous. 

So  much  for  the  normal  orthosilicate  micas.  But  in  the  lepidolites, 
phlogopites,  and  some  muscovites,  the  oxygen  silicon  ratio  is  low ; and 
in  the  lepidolites  especially  it  approximates  more  or  less  closely  to  the 
metasilicate  type.  This  order  of  variation  is  clearly  established,  while 
variations  in  the  opposite  direction,  that  is  toward  excess  of  oxygen, 
may  be  questionable.  If,  however,  in  any  mica  the  oxygen  can  be 
properly  in  excess  of  Si04,  that  excess  may  be  fairly  regarded  as  present 
in  the  group  — A1=0,  which  is  obviously  equivalent  to  Al=F2,  and 
takes  place  with  the  latter  as  a part  of  IF.  Examples  of  this  kind  are 
given  in  one  of  my  former  papers.1  In  all  such  cases  the  system  of 
formulae  proposed  above  applies  perfectly,  and  needs  no  qualification. 
The  variations  in  B/  always  fall  within  its  limits. 

The  lower  values  for  the  silicon -oxygen  ratios  are  explicable  as  follows: 
The  polysilicic  acid  H4Si308,  which,  like  H4Si04  is  tetrabasic,  is  repre- 
sented in  nature  by  orthoclase  and  albite.  In  anorthite  we  have  an 
orthosilicate,  and  its  mixture  with  albite  gives,  as  is  well  known  to  all 
mineralogists,  the  intermediate  tricliuic  feldspars  in  which  pseudo-meta- 
silicate ratios  often  appear.  H4Si308+H4Si04=H8Si40i2== 4H2Si03.  It 
we  assume  a similar  state  of  affairs  among  the  micas,  and  regard  ortho- 
silicates and  poly  silicates  as  isomorphously  miscible,  the  lepidolites 
and  other  low  oxygen  micas  are  completely  accounted  for.  We  have 
then  the  same  system  of  general  formulae  for  all  micas,  the  normal  salts 
Al4(Si04)3  and  Al4(Si308)3  being  the  theoretical  starting  points  for  deri- 
vation. In  every  case  the  composition  of  a mica  becomes  reducible  to 
the  one  general  type,  under  the  proposed  theory  of  substitution.  Repre- 
senting the  groups  Si04  and  Si308  by  the  common  symbol  X,  the  micas 
all  fall  within  limits  indicated  by  the  formulae  A13X31F3,  and  A1X3IF9. 
We  may  test  this  principle  and  the  preceding  formulae  by  application 
to  actual  examples,  taking  the  different  micas  group  by  group. 


1 Am.  Jour.  Sci.,  Aug,,  1887,  p.  131. 


12 


WASHINGTON  LABORATORY. 


| BULL.  64. 


MUSCOVITE. 

This  mica,  the  most  typical  and  most  abundant  of  all,  is  also  the 
simplest  chemically.  It  is  best  represented  by  formula  No.  1,  which, 
in  its  special  application,  becomes  ordinarily  Al3(Si04)3KH2,  with  some 
variation  in  the  ratio  of  K to  H.  In  most  cases  muscovite  contains 
small  amounts  of  magnesia  and  ferrous  iron  $ and  if  these  are  deducted, 
as  shown  in  formula  No.  6,  the  residue  agrees  still  better  with  formula 
No.  1.  Fluorine  is  often  present  in  small  quantities,  and  appears  to 
vary  in  relation  to  hydrogen,  being  the  lowest  when  the  latter  is  high, 
and  the  reverse.  Hence  it  is  probable  that  the  group  A1F2  replaces  H 
rather  than  K.  This  is  shown  more  clearly  among  the  lepidolites,  in 
which  fluorine  reaches  a maximum,  while  the  proportion  of  water  is 
almost  insignificant. 

Some  muscovites,  however,  vary  from  the  normal  compound  in  that 
they  contain  more  silicon  and  less  oxygen ; thus  approaching  somewhat 
to  lepidolite.  These  micas,  which  Tschermak  has  called  u phengites,” 
are  represented  by  him  as  mixtures  of  Al6R/6Si6024  with  H8Sii0O24  in  the 
ratio  of  three  to  one.  It  is  simpler,  however,  to  follow  out  the  analogy 
offered  by  the  feldspar  group,  and  to  assume  the  existence  in  muscovite 
of  the  isomorphous  compound  Al3(Si308)3KH2.  True,  this  compound 
has  not  been  found  by  itself  in  nature,  and  so  far  its  assumption  is 
objectionable.  But  the  compound  H8Si]0O24  is  also  non-existent,  is 
different  in  type  from  ordinary  muscovite,  and  is  not  easily  conceivable 
as  a definite  entity.  The  alternative  which  I offer  for  it  is  therefore,  it 
seems  to  me,  more  philosophical  and  more  satisfactory ; and  it  accounts 
completely  for  all  the  oxygen  variations  in  muscovite.  For  the  sake  of 
brevity,  however,  we  may  well  retain  the  name  of  phengite  in  our 
vocabulary,  and  may  speak  of  micas  containing  the  Si308  group  as 
more  or  less  phengitic. 

In  order  to  show  the  method  of  discussion  which  I have  employed, 
we  may  take  the  four  muscovite  analyses  considered  by  Tschermak.  A, 
muscovite  from  Bengal,  analyzed  by  Blau ; B,  East  Indies,  by  Sipocz ; 
C,  Bothenkopf  in  the  Zillerthal,  by  Sipocz ; D,  Soboth  in  Steiermark, 
by  Lobisch.  Of  these,  C and  D are  phengites. 


A. 

B. 

C. 

I). 

Si02  

45.57 

45.  71 

45.  87 

48.76 

AI2O3 

36.  72 

36.57 

30.  86 

29.  91 

Fe20a 

.95 

1.19 

5. 70 

4.  24 

FeO 

1.28 

1.07 

1.  69 

.41 

MgO 

.38 

.71 

1.56 

2.63 

CaO 

.21 

.46 

.23 

.33 

K20 

8. 81 

9.22 

9.07 

6.83 

Xa20 

.62 

.79 

.54 

2. 31 

Li20 

. 19 

H20 

5.05 

4.83 

4.60 

4.  60 

F 

.15 

. 12 

99.  93 

100.  67 

100. 12 

100.  02 

CLARKE.  J 


A THEORY  OF  THE  MICA  GROUP. 


13 


•Now,  computing  the  molecular  ratios  in  the  usual  way,  uniting  ferric 
oxide  with  alumina,  ferrous  iron  and  lime  with  the  magnesia,  and  con- 
solidating the  alkalies  under  the  general  symbol  R'20,  we  have  the 
following  empirical  formulae  for  the  four  micas : 

A.  Al732Mg3oR/22oH56oF  eSbsgCbiE?* 

B . Al732Mg39R/-2.22H53fiF  gSi 7620.3037° 

C . A1 676M  g6sR  '21 2H5 12  S i 765O2972  • 

D.  Al634Mg78R/220H5l2Si813O302l° 

Regarding  the  fluorine  as  A1F2,  and  uniting  it  and  the  H with  R', 
these  formulae  become,  almost  exactly : 

A.  Al729Mg3oR/783(Si04)753(Si308)2° 

B.  AbagMgsgRbei  (Si 

C . Alfi76Mge6R/724(  Si04)699(  S^Og^. 

D.  Al634Mg7sR'732(Si04)642(Si308)67* 

Combining  the  two  acid  groups  under  the  indiscriminate  symbol  X, 
we  have : 

A.  Al729Mg3oR/783X755. 

B.  Al729Mg39R'76lX766. 

C.  Al«76Mg66R/724X72l. 

D.  . Al634Mg78R/732X699« 

These  are  equivalent  to  the  following  mixtures  of  the  isomorphous 
salts  represented  by  the  general  formulae  6, 3,  and  1,  in  the  fundamental 
system  above  cited : 

A.  10  AlX3Mg3R/3+4  AlX3R'9+238  AhXsR's. 

B.  13  AlX3Mg3R/3+239  AI3X3R?. 

C.  22  AlX3Mg3R'3+218  A13X3R'3. 

D.  26  AIXaMggR's-f  7 AlX3R/9+200  A13X3R'3. 

In  each  case  the  final  formulae  vary  from  the  original  ratios  only  to 
an  extent  which  is  ascribable  to  the  minute  residual  errors  of  calcula- 
tion. The  new  expressions  conform  perfectly  to  the  evidence  of  analysis. 
Eight  other  muscovite  analyses,  similarly  discussed,  gave  strictly 
similar  and  equally  sharp  results. 

LEPIDOLITE. 

In  this  species,  the  most  phengitic  of  all  the  micas,  we  find  little 
water,  high  fluorine,  and  a very  notable  proportion  of  lithia.  It  always 
occurs  with  muscovite,  and  commonly  implanted  upon  the  latter  in 
such  a way  as  to  clearly  indicate  its  later  formation.  In  composition  it 
is  regarded  by  Tschermak  as  a mixture  of  AlfiK6Si6024  with  F24Sii0O8, 
the  former  being  about  half  replaced  by  the  corresponding  Al6Li6Si6024, 
and  the  latter  in  part  by  H8Sii0O2l.  The  objections  to  this  interpreta- 
tion have  already  been  pointed  out. 

Under  the  new  mode  of  interpretation,  lepidolite  becomes  much 
simpler.  In  every  case,  if  we  eliminate  traces  of  magnesia  and  iron, 
as  was  done  under  muscovite,  the  residue  corresponds  sharply  to  a 
mixture  of  the  two  molecules  AlX3R/9  with  Al;,X:iR'j,  X representing 


14 


WASHINGTON  LABORATORY. 


[BULL.  64. 


Si308  and  Si04  indiscriminately.  In  the  purest  lepidolites  these  mole- 
cules are  in  the  ratio  1 : .1,  corresponding  to  A12X3R'6;  but  in  general 
the  second  molecule  is  slightly  in  excess,  due  to  small  admixtures  of 
normal  muscovite.  In  the  discussion  of  fourteen  published  analyses 
of  lepidolite  the  ratio  Si308:Si04  varies  from  1 : 1 to  1 : 3;  and  the  sum 
of  Li+A1F2  appears  to  be  directly  related  to  the  proportion  of  Si3Oe. 
In  brief,  expanding  the  general  formulae  given  above,  typical  lepidolite 
may  be  expressed  by  the  two  compounds  Al3(Si04)3KHLi  and 
Al(Si308)3K3Li3(AlF2)3  in  equal  molecules.  All  the  variations  may  be 
accounted  for  by  admixtures  of  muscovite,  with  sometimes  a trivial 
amount  of  the  magnesium  or  iron  salt,  No.  6,  as  an  impurity. 

For  purposes  of  illustration,  four  of  the  lepidolite  analyses  may  be 
considered  in  detail,  as  follows:  E,  from  Rozena,  by  Berwerth,1  F, 

Juschakova,  by  Rammelsberg;2  G,  Schuttenhofen,  by  Scharizer;3  H, 
white  lepidolite  from  Norway,  Maine,  by  Riggs.4 


. 

E. 

F. 

Gr. 

1 

H. 

Si02  ------------ 

50. 98 

50.  96 

49. 26 

49. 52 

ai2o3 

27. 80 

22.20 

25. 26 

28.  80 

Fe203 

.40 

Mn203  

5.  38 

MnO  

.85 

.07 

.24 

FeO 

.05 

.84 

MgO 

. 02 

CaO 

. 13 

k2o 

10. 78 

11. 39 

13.85 

12. 63 
. 13 

;Na20  

.32 

.35 

T.i.O 

5.88 

5.65 

5.38 

3.87 

h2o 

.96 

1.76 

1. 72 

F 

7.  88 

8.58 

5.68 

5.18 

p2Og 

.05 

SnO. 

.06 

Less  0 

104. 38 
3. 32 

104.48 
3. 61 

103. 29 
2. 38 

102. 71 
2. 18 

101.06 

100.  87 

100. 91 

100.  53 

Disregarding  trivial  impurities,  and  computing  the  ratios  as  before, 
we  have  from  these  analyses  the  subjoined  empirical  expressions: 

E.  Al347K230l<i392Hi06(AlF2)207(Si3O8)l8l(SiO4)306. 

F . A1.28oK252Li376(  AlF2)22fi(Si308)  212(Si04)2l2. 

G.  Al345R,/24K25oLi358Hi96(  AIF2)  149(  Si3Os)  I ,%(  Si04)353« 

H . A1434R'  /7K272Li268Hi92(  A1F  2 ) 136(  S^Os)  141  ( SiO4)403* 

Condensing,  these  become: 

E.  Al347R/935X487. 

F.  Al28oR/854X424. 

G.  Al345R//24R/95sX509. 

H.  A1434R//7R/858X544. 


1 See  Tschermak’s  paper,  1.  c. 

2 Wiedemann’s  Annalen,  vol.  7,  p.  143. 


! Zeitschr.  Rryst.,  vol.  13,  p.  467. 
A Am.  Jour.  Sci.,  Nov.  1886. 


CLARKE.] 


A THEORY  OF  THE  MICA  GROUP. 


15 


Whence  we  get,  very  nearly: 

E.  70  AlX3R'9+92  A13X3R'3 

F.  71  AlX3R'9+70  A13X3R'3. 

G.  8 AlX3R"3R'3+75  AlX3R/9-f-87  AUXjjRV 

H.  2 AlXaR'^RV^  A1X3R'9+127  AlaXaR's. 

Two  other  highly  fluoriferous  lithia  micas,  cryophyllite  and  zinn- 
waldite,  may  properly  be  considered  here.  For  the  former  we  have 
Riggs’s  analysis,  and  for  the  latter,  analyses  by  Berwerth  and  Rammels- 
berg.  From  these  analyses  we  get  the  following  empirical  formula: 
1,  Riggs,  cryophyllite;  2 and  3,  Berwerth  and  Rammelsberg,  zinn- 
waldite. 

1.  Ali86Fe//94K256Ui3-24H]46(AlF2)i78;(Si308)227(Si04)l85. 

2.  Al.239Fe//i86K236Li2i8HI02(AlF2)20y(Si3O8)l51(SiO4)3i2. 

3.  A1244F Q1* ifjj K2 12U224 Uj  ] 6(  A1F2)20o( 8i30s)l56(  SiO4)306» 

Condensiug  these  formula  they  become : 

1.  Al186Fe94R,904X4i2. 

2.  Al239Fei86R/765X463* 

3.  Ah-HFe^R^saX^z. 

Expanding  again,  these  formulse  give : 

1.  31  (AlX3Fe//3R/3)+81(AlX3R/9)+25(Al3X3R/3). 

2.  62  “ +49  “ +43 

3.  56  “ +53  “ +45  “ 

The  component  molecules  here  correspond  essentially  to  Nos.  6,  3, 
and  1 of  the  fundamental  series,  the  last  one  in  each  expression  being 
muscovite.  Whether  the  separate  components  of  R'  and  X can  be 
distributed  with  certainty  among  the  several  molecules  is  an  outstand- 
ing question;  but  not,  I believe,  an  unanswerable  one. 

PHLOGOPITE. 

In  order  to  ascertain  the  composition  of  this  mica  I have  discussed 
the  four  analyses  cited  by  Tschermak  (1.  c.),  and  three  of  Rammels- 
berg’s.1  All  of  these  are  fluoriferous,  and  all  but  one  are  phengitic,  the 
exception  in  the  latter  case  being  the  Edwards,  N.  Y.,  mineral,  which 
Tschermak  regards  as  somewhat  altered.  I have  also  considered  the 
new  phlogopite  from  Edwards,  recently  described  by  Penfield,2  which 
is  remarkable  as  being  free  from  fluorine. 

In  general,  phlogopite  agrees  closely  with  the  formula  AlX3Mg3B/3, 
but  there  are  often  variations  which  are  not  easy  to  explain,  and  which 
are  greater  than  can  be  accounted  for  by  presumable  errors  of  analysis. 
They  may  be  due  in  part  to  impurities  arising  from  the  great  altera- 
bility  of  the  mineral;  but  I am  inclined  to  trace  the  difficulties  toother 
sources. 

1 Wiedemann’s  Annalen,  vol.  9,  p.  129.  2 Am.  Jour.  Sci.  (3),  vol.  36,  p.  329. 


16 


WASHINGTON  LABORATORY. 


[BULL.  64. 


In  order  to  satisfy  the  conditions  of  the  formulae  proposed  by  me,  it 
is  necessary  that  the  aluminum  atoms,  apart  from  A1F2,  shall  be  in 
number  at  least  one- third  of  X ; but  in  several  phlogopites  the  alum- 
ina is  too  low  to  fulfill  this  requirement,  and  the  difficulty  is  best 
obviated  by  assuming  an  MgF  group  in  place  of  A1F2.  In  Penfield’s 
phlogopite,  however,  there  is  no  fluorine,  and  yet  the  alumina  is  con- 
siderably— about  two  per  cent- — too  low.  If  we  suppose  in  his  mineral, 
which  came  from  a talc  mine,  a small  admixture  of  talc,  the  residue 
agrees  with  the  theoretical  formula,  X being  wholly  Si04  ; but  if  that 
impurity  is  absent  we  must  assume  that  the  mica  differs  from  ordinary 
phlogopite  by  containing  the  group  — Mg  — OH  instead  of  the  usual 
MgF.  The  composition  of  the  mineral  then  reduces  to  the  uniform 
type.  I am  now  disposed  to  believe  that  phlogopite  differs  from  the 
other  micas  in  that  it  contains  these  special  groups  MgF  and  MgOH, 
both  as  part  of  R' ; but  the  supposition  is  not  yet  fully  justified.  It  is, 
however,  I think,  susceptible  of  experimental  investigation,  and  a lab- 
oratory research  upon  the  problem  is  now  being  carried  out  under  my 
direction.  Apart  from  that,  the  supposition  is  strengthened  by  the 
composition  of  certain  vermiculites,  some  of  which  have  certainly  been 
formed  by  the  alteration  of  phlogopite.  Three  of  these  interesting 
minerals  are  represented  fairly  well  by  the  subjoined  formulse,  in  which 


ferric  iron,  present  in 
alumina. 

small  quantities,  has 

been  reckoned  with  the 

Si04  — (MgOH)3  Si04  — ) 

Si04  — MgH 

/ 

/ >Mg3 

/ 

A1 — Si04  — A1 

A1 — Si04—  S 

Al  — Si04-MgH 

\ 

\ 

\ 

Si04  = AI 

Si04=  A1 

Si04  = Al 

-j-3H20. 

+3H20. 

+3H20. 

Dudleyite. 

Culsageeite. 

Jefferisite. 

It  is  by  no  means  certain  that  the  vermiculites  are  so  simple  in  compo- 
sition or  so  definite  as  these  symbols  would  seem  to  indicate ; but  the 
formulae  are  decidedly  suggestive,  and  they  show  how  clearly  the 
relations  between  the  micas  and  their  derivatives  may  be  expressed. 

THE  FERRO-MAGNESIAN  MICAS. 

This  group  of  micas,  which  includes  biotite,  lepidomelane,  annite, 
haughtonite,  siderophyllite,  and  other  supposed  species,  is  apparently 
quite  complex.  In  place  of  magnesia,  ferrous  iron  is  often  predominant ; 
in  the  lepidomelanes,  ferric  iron  replaces  aluminum,  and  in  forty-four 
out  of  the  fifty-six  analyses  discussed,  the  oxygen  was  in  excess  of 
Si04.  Only  seven  of  these  micas  appeared  to  be  phengitic ; and  ohly 
sixteen  of  the  analyses  reported  fluorine  in  small  quantities.  In  six 
instances  AlO  and  A1F2,  were  both  absent. 

For  thirty-four  of  the  micas  in  this  group,  formulae  could  be  easily 
computed  upon  the  lines  already  followed ; that  is,  in  each  case  the 


CLARKJE.J 


A THEORY  OF  THE  MICA  GROUP. 


17 


composition  was  represented  by  a mixture  of  AlXgE'^E'g  with  AIXsE'g 
and  AI3X3R/3,  the  second  or  third  of  these  molecules  being  occasionally 
absent.  Among  the  lepidomelanes  there  was  an  approximation  to  a 
distinctively  muscovitic  type ; and  in  two  cases  formula  No.  4,  A13X3E"E, 
seemed  to  apply.  With  each  mica  an  attempt  was  made  to  determine 
the  proportions  of  the  several  admixed  molecules ; but  the  results, 
although  numerically  conformable  to  the  general  theory,  were  not  abso- 
lutely conclusive.  The  chief  difficulty  lay  in  the  uncertainty  attaching 
to  the  water  determinations,  upon  which  the  question  of  oxygen  excesses 
depends.  Since  water  has  a low  molecular  weight,  a small  error  in  its 
estimation  becomes  relatively  large  in  the  molecular  ratios,  and  two 
sorts  of  errors  are  presumable:  First,  an  excess  of  water  may  be 
inclosed  mechanically  in  the  material  analyzed,  and  secondly,  a deter- 
mination by  simple  ignition  is  likely  to  be  too  low  because  of  the  oxida- 
tion of  ferrous  iron.  If  these  errors  occur  together,  they  obviously 
tend  to  compensate  each  other  ; but  either  one  alone  seriously  affects 
the  co-efficient  of  E',  and  appears  in  the  ratio  between  A13X3E'3  and 
A1X3E'9. 

In  twenty-two  of  the  fifty-six  analyses,  however,  the  symbol 
AD^E^E^  failed  to  account  for  all  the  bivalent  metals,  iron  and  mag- 
nesium. In  these  cases  E"  was  in  excess  of  E',  and  it  became  necessary 
to  make  use  of  formula  Xo.  7,  Al2(Si04)6E/,9.  With  the  aid  of  this 
expression  all  the  ferro-magnesian  micas,  without  a positive  exception, 
including  the  phlogopites,  were  resolvable  into  mixtures  of  A13X3E,3, 
AlXgE'g,  and  AbXcE'V  Upon  this  basis  formula  Xo.  6 becomes  useless, 
for  •Al^X3]VIg3E/3  is  evidently  equivalent  to  a mixture,  in  equal  molecules, 
of  AlXgE'g  and  Al2X6Mg9.  Ail  micas,  th  en,  so  far  as  the  analyses  are 
authentic,  may  be  represented  as  mixtures  of  the  molecules  1,  3,  and 
7,  these  being  symbols  of  one  and  the  same  general  type.  The  magne- 
sium (or  ferrous)  salt  thus  assumed,  moreover,  is  not  absolutely  hypo- 
thetical; for,  with  six  molecules  of  water  of  crystallization  added,  it 
approximates  to  certain  individuals  of  the  chlorite  group.  Some  exam- 
ples of  penninite,  for  instance,  approach  rather  closely  to  the  composi- 
tion Al2(Si04)6Mgg . 6H20,  which  requires  38.71  of  silica,  10.97  alumina, 
38.71  magnesia,  and  11.61  water.  We  have  thus  a clue  to  the  constitu- 
tion of  the  chlorites,  by  means  of  which  they  may  be  brought  into 
simple  relation  with  the  micas.  This  problem  is  now  under  investigation, 
and  I can  only  state  as  a probability  that  most  of  the  chlorites,  if  not 
all,  may  be  represented  as  mixtures  of  three  fundamental  molecules, 
A12X6E"9,  6H20 ; A1X3E"3H3,  3H20,  and  Al2X3(MgOH)fi.  I hope  to 
speak  more  positively  upon  this  subject  before  long;  at  present  I need 
only  point  out  that  two  of  these  molecules  are  simple  hydrates  of  Xos. 
6 and  7,  while  the  third  is  covered  by  the  general  symbol  Xo.  3,  in  which 
E'g  becomes  (MgOH)6.  The  easy  alterability  of  garnet,  Al2(Si04)3E//3 
into  mica  and  chlorite,  is  a suggestive  bit  of  evidence  bearing  upon 
these  expressions. 

Bull.  64 2 


18 


WASHINGTON  LABORATORY. 


[BULL.  61- 


MARGARITE. 

Whether  this  species  is  to  be  considered  as  a true  mica  or  not,  is 
perhaps  an  open  question.  Its  composition  is  relatively  simple,  and  is 
represented  by  the  empirical  formula  H2CaAl4Si2Oi2.  Structurally,  this 
may  be  written  in  two  distinct  ways,  as  follows: 

OH  Si04E(A10)2H. 

/ _ / 

Al  — Si04  — CaH  or  Ca 

^SiO.E  (AlO),  >VSi04E(A10)2H. 

The  first  of  these  symbols  derives  the  compound  from  the  normal 
aluminum  salt,  and  indicates  a similarity  of  type  with  the  micas  proper. 
The  second  assumes  a normal  calcium  salt  as  the  point  of  derivation  j 
and  I am  unable  as  yet  to  assign  a distinct  preference  to  either  ex- 
pression. A careful  study  of  the  genesis  and  associations  of  margarite 
may  determine  which  of  the  two  formulae  is  the  better.  Possibly  the 
occurrence  of  the  mineral  in  such  mixtures  as  euphyllite,  and  the 
probable  existence  of  a similar  barium  salt  in  cellacherite  points  to  the 
first  of  the  two  formulae  as  the  better.  The  common  occurrence  of 
margarite  with  diaspore  also  points  in  the  same  direction.  Corundophi- 
lite,  which  occurs  associated  with  both  margarite  and  diaspore,  also 
reduces  to  a type  resembling  the  first  margarite  formula. 


THE  CLINTONITE  GROUP. 


These  minerals,  the  so-called  u brittle  micas,”  have  also  been  discussed 
by  Tschermak,1  who  includes  under  this  heading  seybertite,  brandisite, 
xanthophyllite,  ehloritoid,  masonite,  ottrelite,  sismondine,  and  sapphir- 
ine.  Physically,  they  are  closely  related  to  the  micas  proper,  and  to 
margarite  in  particular ; but  chemically  they  are  much  more  basic.  The 
first  three  species  Tschermak  regards  as  mixtures  of  the  hypothetical 
compounds  H2CaMg4Si30i2  and  H2CaMgAl6Oi2;  to  ehloritoid  he  assigns 
the  composition  H2Si2Fe//207,  x H2A1407,  and  sapphirine  he  represents 
by  the  formula  Si2Mg206-bAl6Mg2On. 

Using  the  analyses  cited  by  Tschermak,  I find  that  all  these  minerals, 
with  the  possible  exception  of  sapphirine,  may  be  represented  by  the 
general  expression 

O 


/ >R" 

Al-0 


\ 

Si04  = 


R'3, 


which  is  clearly  and  directly  related  to  the  formulae  already  assigned 
to  the  micas  and  to  margarite,  and  in  which  the  mode  of  union  of  Ru 
with  Al,  when  R"r=Mg,  suggests  the  common  association  of  mem- 
bers of  this  group  with  spinel.  In  seybertite  we  have  a mixture  of 


' 1 Zeitsckr.  Kryst.,  vol.  3,  p.  496. 


CLABKE.] 


A THEORY  OF  THE  MICA  GROUP. 


19 


A102R"Si04(Mg0H)3  with  Ai02R"Si04(  A10)3,  R"  being  partly  Oa  and 
partly  Mg.  In  brandisite  we  have  a similar  constitution,  with  about  one- 
fourth  of  R"  replaced  by  H2.  In  chloritoid,  R"=Fe  and  R/3=H2(A10) ; 
and  sismondine  is  similar,  with  R'3  possibly  replaced  in  part  by  Al.  The 
compound  A102MgSi04(A10)3,  found  in  seybertite,  is  a rough  approxi- 
mation to  sapphirine,  which  mineral  possibly  has  this  composition  plus 
some  impurities  as  yet  unidentified.  A wider  range  of  analyses  is 
needed  in  order  to  establish  these  formulae  completely;  but  they  seem 
to  have  distinct  advantages  over  the  formulae  proposed  by  Tschermak. 

CONCLUSIONS. 

All  the  micas,  vermiculites,  chlorites,  margarite,  and  the  ciintonite 
group  may  be  simply  represented  as  isomorphous  mixtures,  every  con- 
stituent being  a substitution  derivative  of  normal  aluminum  polysilicate 
or  orthosilicate.  To  the  latter  compound  a structure  may  be  assigned 
somewhat  different  in  form  from  the  one  I have  chosen,  without  affect- 
ing in  any  notable  way  the  general  system  adopted.  Upon  this  basis 
all  the  minerals  named  are  reducible  to  the  same  general  type,  which 
accounts  for  observed  isomorphisms,  and  for  the  relations  of  the  micas 
to  other  species,  with  fewer  assumptions  of  hypothetical  compounds 
than  are  necessary  under  other  known  schemes  of  interpretation.  In 
most  cases  the  evidence  is  clear,  direct,  and  conclusive ; in  other  cases, 
few  in  number,  it  is  at  present  somewhat  obscure.  It  may  be  claimed, 
without  extravagance,  that  the  formulae  have  the  merit  of  suggestive- 
ness, and  that  they  form  a scientific  basis  for  future  research. 


A PLATINIFEROUS  NICKEL  ORE  FROM  CANADA 


By  F.  W.  Clarke  and  Charles  Catlett. 


During  the  autumn  of  1888  we  received,  through  two  different  chan- 
nels, samples  of  nickel  ores  taken  from  the  mines  of  the  Canadian 
Copper  Company  at  Sudbury,  Ontario.  From  one  source  we  obtained 
two  masses  of  sulphides,  to  be  examined  for  nickel  and  copper ; from 
the  other  source  came  similar  sulphides,  together  with  a series  of  soil 
and  gravel-like  material,  seven  samples  in  all.  In  the  latter  case  an 
examination  for  platinum  was  requested,  and  in  five  of  the  samples  it 
was  found,  the  gravel  above  mentioned  yielding  74.85  ounces  of  metals 
of  the  platinum  group  to  the  ton  of  2,000  pounds.  At  the  outset  of 
the  investigation  we  were  decidedly  incredulous  as  to  the  existence  of 
platinum  in  such  ores;  but  the  discovery  of  sperrylite  by  Mr.  Wells 
in  material  from  the  same  mines  gave  our  work  a wholesome  stimulus, 
and  the  assays  were  carefully  carried  through. 

The  sulphide  ores  submitted  to  us  from  Sudbury  were  all  of  similar 
character.  They  consisted  of  mixed  masses,  in  which  a gray  readily 
tarnishing  substance  was  predominant,  with  some  chalcopyrite,  possibly 
some  pyrite,  and  a very  little  quartz.  Two  samples  were  examined  in 
mass ; one  gave  31.41  per  cent  of  nickel  with  a little  copper,  the  other 
gave  35.39  per  cent  of  nickel  and  5.20  of  copper.  The  nickel  mineral 
itself  proved  to  be  a suphide  of  nickel  and  iron,  and  as  ores  of  that 
composition  are  not  common,  it  was  thought  desirable  to  examine  the 
substance  further. 

As  above  stated,  the  nickel  mineral  is  the  predominating  constituent 
of  the  masses  submitted  for  examination.  It  is  steel  gray,  massive,  and 
exceedingly  alterable  in  the  air,  and  its  specific  gravity,  determined  by 
jjycnometer,  is  4.541.  An  analysis  of  carefully  selected  material  gave 
the  following  results : 


Ni.. 

Fe.. 

Si02 

Cu.. 

S... 


41.96 
15. 57 
1.0*2 
.62 
40. 80 


99.97 

Neither  cobalt  nor  arsenic  could  be  detected. 

The  foregoing  figures  work  out  sharply  into  the  ratio  R : S : : 4 : 5 ; and 
approximately  into  the  formula  Ni3FeS5.  If  we  deduct  silica,  together 

20 


Ccatlett!P]  NICKEL  ORE  FROM  CANADA.  21 

with  the  copper  reckoned  as  admixed  chalcopyrite,  and  recalculate  the 
remainder  of  the  analysis  to  100  per  cent,  we  have  the  following  figures  : 


As  found. 

Calc,  as 
Xi3FeSs. 

m 

j 43. 18 

44.6 

Fe 

! 15.47 

14.4 

S 

41.35 

41.0 

100.  00 

100.0 

In  short,  the  mineral  has  the  composition  Ni4S5,  with  about  one-fourth 
of  the  nickel  replaced  by  iron.  The  only  known  species  with  which  this 
agrees  is  Laspeyres’s  polydymite,  of  which  the  Sudbury  mineral  is  evi- 
dently a ferriferous  variety.  What  relations  it  may  bear  toward  bey- 
richite,  pyrrhotite,  etc.,  is  as  yet  a matter  of  considerable  uncertainty. 
Probably  in  most  cases  the  nickeliferous  constituent  of  pyrrhotite  is 
millerite,  but  other  sulphides,  like  the  polydymite,  may  perhaps  occur 
also. 

The  polydymite  which  was  selected  for  the  above  analysis  came  from 
the  mass  in  which,  in  average,  35.39  Ni  and  5.20  Cu  had  previously  been 
found.  The  mass  weighed  several  kilograms,  and  was  remarkably  free 
from  quartz.  The  same  mass,  with  two  smaller  pieces  resembling  it, 
were  also  examined  for  platinum,  by  the  following  method : One  assay 
ton  of  the  finely  ground  ore  was  treated  with  nitric  acid  until  all  or 
practically  all  of  the  sulphides  had  been  dissolved.  The  dried  residue 
was  then  assayed  in  the  usual  manner : except  that,  to  facilitate  cu- 
pellation,  a little  pure  silver  was  introduced  into  the  lead  button.  From 
the  final  bead  the  silver  was  dissolved  out  by  sulphuric  acid,  leaving 
the  platinum  in  a finely  divided  gray  powder.  The  latter  dissolved 
easily  in  aqua  regia,  and  gave  all  the  reactions  needful  to  identify  it 
thoroughly.  The  results  were  as  follows,  “A”  representing  the  large 
mass  in  which  the  polydymite  was  determined : 

Per  cent. 


A,  2.55  ounces  Pt  to  the  ton,  or 0.0087 

B,  1.8  ounces  Pt  to  the  ton,  or 0060 

C,  7 ounces  Pt  to  the  ton,  or 0240 


That  the  metal  weighed  was  nearly  all  platinum  is  certain ; but  it 
may  have  contained  small  amounts  of  other  metals  of  the  same  group. 
The  material  separated  was  not  sufficient  to  warrant  a search  for  the 
rarer  associates  of  platinum.  Probably  the  platinum  exists  in  the  ore 
as  sperrylite,  although  this  point  was  not  proved.  The  amount  of  plati- 
num in  the  mass  most  thoroughly  examined  would  require,  to  form 
sperrylite,  only  about  0.007  per  cent  of  arsenic,  which  is  too  small  a 
quantity  for  detection  by  ordinary  analysis.  That  platinum  should 
exist  in  appreciable  quantities  in  an  ore  of  such  character  is  something 
quite  extraordinary.  Whether  it  could  be  profitably  extracted  is  an 
open  question. 


A NEW  OCCURRENCE  OF  GYROLITE. 


By  F.  W.  Clarke. 


In  the  autumn  of  1888,  during  a visit  to  the  New  Almaden  Quick- 
silver Mine  in  California,  Dr.  D.  T.  Day,  of  the  U.  S.  Geological  Survey, 
was  shown  specimens  of  a mineral  which  was  locally  supposed  to  be 
white  fluor-spar.  It  occurred  in  well- developed  crystals  lining  crevice 
veins  in  the  mine,  and  was  easily  recognizable  as  apophyllite.  Dr. 
Day  secured  a good  series  of  the  specimens,  and  finally  turned  them 
over  to  me  for  examination.  The  largest  crystals  were  about  two 
centimeters  in  diameter,  and  fairly  transparent,  and  grew  out  of  crys- 
talline masses  of  considerable  thickness,  the  exposed  definite  faces 
nearly  meeting  at  the  center  of  the  seam  or  vein.  All  of  the  specimens 
were  saturated  with  bituminous  matter,  but  except  for  that  staining 
they  were  quite  colorless. 

In  several  of  the  specimens  received  the  wall  of  the  seam  was  dis- 
tinctly shown,  and  between  it  and  the  crystalline  apophyllite  there  was 
a fibrous  layer  from  one  to  three  centimeters  in  thickness.  That  layer 
was  also  colorless,  except  for  bituminous  staining,  and  on  account  of  its 
relations  to  the  apophyllite  it  appeared  to  deserve  investigation.  A 
sufficient  quantity  of  the  material  having  been  selected,  it  was  digested 
for  about  twenty-four  hours  with  ether  in  order  to  cleanse  it  from  bitu- 
men, and  then  analyzed.  I give  the  result  in  comparison  with  How’s 
figures  for  a Nova  Scotia  gyrolite : 


Clarke. 

How. 

h2o  

14.60 

15.05 

Si02  

52.54 

51. 90 

A1203 

1. 27 

Fe203  

j 0.71 

CaO 

29.  97 

29.  95 

MpO 

0. 08 

k2o 

1.56 

1.60 

Xa20 

0. 27 

F 

0. 65 

Less  O 

100. 30 
0.  27 

99.  85 

100.03 

22 


23 


clarke.]  A NEW  OCCURRENCE  OF  GYROLITE. 

It  will  at  once  be  seen  that  the  two  analyses,  except  for  the  small 
amount  of  fluorine,  coincide  quite  sharply,  and  establish  the  New  Alma- 
den  mineral  as  gyrolite.  The  Nova  Scotian  gyrolite  is  also  associated 
with  apophyllite,  from  which  species  How  supposed  it  to  be  derived.1 
In  the  present  instance,  however,  the  relative  position  of  the  two  min- 
erals in  the  vein  suggests  that  the  gyrolite  is  the  older ; and  that  the 
apophyllite  may  have  been  formed  from  it  by  a partial  solution  and 
redeposition  of  its  material  through  the  agency  of  waters  containing 
alkaline  fluorides.  The  gyrolite  is  obviously  not  absolutely  pure,  but 
it  agrees  approximately  with  the  formula  Ca2Si308 . 3H20.  Its  chemi- 
cal structure  and  relations  to  apophyllite  are  not  altogether  clear. 


1 Am.  Jour.  Sci,  (2),  vol.  32,  p.  13. 


ANALYSES  OF  THREE  DESCLOIZITES  FROM  NEW  LOCALITIES. 


By  W.  F.  Hillebrand. 


1.  MAYFLOWER  MINE,  BALD  MOUNTAIN  MINING  DISTRICT,  BEAVER- 
HEAD COUNTY,  MONT. 

Through  Messrs.  W.  H.  Beck  and  George  E.  Lemon,  of  Washington, 
D.  0.,  was  received  about  a year  ago  for  examination  a large  lump  of 
friable,  un crystallized  material,  having  a dull  yellow  to  pale  orange 
color,  and  consisting  chiefly  of  a vanadate,  but  carrying  a large  per- 
centage of  gangue.  Two  samples  as  pure  as  could  be  selected  from 
different  parts  of  the  lump  were  analyzed  with  the  following  results: 


e ‘ 

I. 

II. 

Mean. 

Molecular  ratios. 

PbO 

56.  02 

55.  84 

55. 93 

. 2508  ^ 

CuO 

1.16 

1. 13 

1.15 

. 0145  1 

> . 4718  4. 02 

FeO 

0.  70 

0.70 

0. 70 

.0097| 

ZnO 

15.  96 

15.  91 

15.94 

. 1968 J 

V206 

20.  80 

20.80 

As205 

0. 32 

0. 32 

. 1140 1 

.0014  >.1173  1.00 

P206 

0. 27 

0.  27 

. 0019  J 

H20 

4.  37 

4.  36 

4.  37 

. 2428  2. 07 

Si02  ............ 

0. 20 

0. 16 

0. 18 

CaO 

0. 10 

0. 10 

MgO 

0.  06 

0.06 

99. 82 

From  I 27.62  per  cent  of  gangue  insoluble  in  cold  dilute  nitric  acid 
has  been  deducted,  and  from  II  22.20  per  cent ; manganese  was  pres- 
ent in  the  gangue  in  small  quantity,  apparently  as  pyrolusite,  but  it 
was  not  dissolved  by  the  acid.  The  insoluble  portion  was  found  also 
to  retain  very  small  quantities  of  lead  and  zinc,  which  were  estimated 
and  included  in  the  analysis  as  probably  belonging  to  the  vanadate. 
The  water  had  to  be  estimated  indirectly  by  deducting  from  the  total 
amount  of  water  afforded  by  the  dried  mixture  of  vanadate  and  gangue 
that  belonged  to  the  latter  alone,  which  was  found  as  follows : The 
mixture,  dried  at  100°  C.,  was  dissolved  in  cold  dilute  nitric  acid,  and 
the  insoluble  matter  collected  in  a Gooch  crucible  was  dried  at  the  same 
temperature  and  then  ignited.  The  loss  on  ignition  gave  the  water  in 
24 


HILDEBRAND.  ] 


ANALYSES  OF  THREE  DESCLOIZITES. 


25 


the  gangue,  there  being  no  ferrous  iron  in  the  latter  to  influence  the 
result.  The  traces  of  Si02,  CaO,  and  MgO  may  be  neglected  as  proba- 
bly derived  from  the  gangue.  The  water,  it  will  be  noticed,  is  double 
that  required  by  descloizite,  R2(0H)V04,  but  in  view  of  the  liability  to 
error  inherent  in  the  method  of  water  estimation  employed,  this  is  not 
deemed  sufficient  cause  for  separating  the  mineral  from  descloizite, 
although  the  close  agreement  of  the  two  water  determinations,  made 
as  they  were  on  samples  containing  different  proportions  of  gangue, 
would  indicate  the  correctness  of  the  formula  2[R2(0H)V04]  + H20. 

Other  specimens  have  since  been  received  from  the  above-named 
persons  in  which  the  earthy  vanadate  was  associated  sometimes  with 
compact  cerussite  and  galena  in  process  of  alteration.  A dull  reddish 
substance  which  constituted  a part  or  even  the  whole  of  some  lumps 
contained,  besides  silica,  iron  and  some  antimony  in  an  oxidized  condi- 
tion, but  carried  little  or  no  vanadium. 

Prof.  F.  A.  Genth  has  already  called  attention1  to  the  occurrence  of 
vanadinite  and  probably  of  descloizite  in  the  Bald  Mountain  mine, 
Beaverhead  County,  Mont.  His  specimens,  however,  showed  the  sup- 
posed descloizite  as  a pale  brownish  crystalline  coating  on  yellow 
ferruginous  quartz,  whereas  the  present  mineral  shows  no  evidence  of 
crystalline  structure. 

2.  COMMERCIAL  MINE,  GEORGETOWN,  GRANT  COUNTY,  N.  MEX. 

This  is  one  of  the  most  interesting  occurrences  of  descloizite  known, 
because  of  the  extreme  brilliancy  of  coloring  of  the  mineral.  The  ore 
bodies  in  the  Commercial  mine,  as  well  as  in  the  adjoining  MacGregor 
and  Naiad  Queen  mines,  occur  in  limestone  immediately  under  an  over- 
lying  slate,  and  appear  to  narrow  in  depth  where  certain  eruptive  dikes 
cut  through  the  lime,  as  Mr.  Macintosh,  foreman  of  the  Commercial 
mine,  informed  me.  The  absence  of  the  superintendents  of  the  several 
mines  and  the  very  brief  visit  I was  forced  to  make  prevented  obtain- 
ing more  certain  and  detailed  information. 

In  places  where  the  rock  is  most  fractured  and  crushed  the  descloi- 
zite appears  in  greatest  quantity  and  finest  condition  as  an  incrusta- 
tion on  quartz,  often  covering  large  surfaces,  and  in  color  varying  from 
yellow  through  all  shades  of  orange-red  to  deep  reddish  brown,  the 
last-named  colors  predominating.  The  black  color  so  frequent  in 
descloizite  from  Lake  Valley,  N.  Mex.,  caused  by  a superficial  coat- 
ing or  admixture  of  pyrolusite,  is,  so  far  as  my  observation  extended, 
wanting,  hence  specimens  from  Georgetown  are  likely  to  be  much 
sought  after  for  their  showy  appearance.  A specimen  in  one  of  the 
banks  at  Silver  City,  N.  Mex.,  taken  from  one  of  the  Georgetown 
mines,  resembled  a stalactite  in  form.  It  was  probably  fully  three  feet 
in  height  by  six  to  eight  inches  or  more  in  diameter,  and  was  deep 
reddish  brown  in  color. 


1 Proc.  Am.  Phil.  Soc.,  1887,  vol.  24,  p.  38. 


26 


WASHINGTON  LABORATORY. 


[bull.  64. 


The  incrustations  are  for  the  greater  part  distinctly  crystalline  and 
are  generally  made  up  of  aggregates  of  more  or  less  globular  forms  of 
a size  ranging  from  microscopic  to  a diameter  of  one  or  two  millimeters. 
Each  of  these  is  composed  of  a great  number  of  apparently  flat  crystals, 
intergrown,  and  projecting  sufficiently  from  the  surface  to  give  brilliant 
reflections  when  observed  under  the  lens,  and  to  the  naked  eye  a frosted 
appearance  where  the  globular  growths  are  largest.  The  richest  reddish 
brown  color  is  always  coincident  with  this  development  in  size.  The 
globular  character  changes  frequently  to  acicular.  In  such  cases  the 
incrustation  seems  to  have  originally  formed  on  bunches  of  radiating 
acicular,  almost  colorless,  vanadinite,  which  frequently  appears  thus 
coating  the  quartz  and  running  under  the  descloizite  incrustations. 
Sometimes  the  vanadinite  has  entirely  disappeared,  and  then  there  may 
be  a hollow  through  the  center  of  the  descloizite  needle. 

The  occurrence  of  vanadate  of  lead  in  the  MacGregor  mine  at 
Georgetown  has  been  noticed  by  Professor  Genth  (1.  c.,  p.  38).  The  specific 
gravity  of  the  mineral  was  not  determined ; the  hardness  is  about  3.5; 
the  color  of  the  powder  is  orange-yellow.  An  analysis  gave  the  follow- 
ing results  after  deducting  11.91  per  cent  of  insoluble  matter,  almost 
entirely  quartz : 


Molecular  ratios. 

PbO 

CuO 

FeO 

ZnO 

v206 

A8205 

p206 

h2o 

Cl 

Si02 

CaO  

MgO 

56.01 
1.05 
0.07 
17.73 
20.44 
0.  94 
0.  26 
2. 45 

0.  04 

1.  01 
0.  04 
0.  03 

100.07 

. 2512 , 

. 0132 

> . 4843  .4788  4.12 
.0010 [ 

.21891 

.11191 

.0041  !>.  1178  .1162  1.00 
.0018] 

. 1361  1361  1. 17 

.0011 

The  third  column  of  molecular  ratios  gives  those  values  after  allow- 
ing for  admixed  vanadinite  calculated  on  the  basis  of  the  chlorine 
found.  A further  correction  has  probably  to  be  made  for  an  admixed 
soluble  hydrous  (zinc  ?)  silicate,  which  might  make  the  ratio  approxi- 
mate more  closely  to  4 : 1 : 1. 

% 

3.  LUCKY  CUSS  MINE,  TOMBSTONE,  COCHISE  COUNTY,  ARIZ. 

Mr.  W.  F.  Staunton,  superintendent  of  the  Tombstone  Mining  and 
Milling  Company,  and  Mr.  Frank  C.  Earle,  assay er  at  Tombstone, 
kindly  placed  at  my  disposal  for  examination  specimens  of  a vanadium 
mineral  the  identity  of  which  had  not  been  established.  It  was  found 


IIILLEBRAXD.] 


ANALYSES  OF  THREE  DESCLOIZITES. 


27 


in  the  Lucky  Cuss  mine  as  an  incrustation,  sometimes  half  an  inch 
thick,  on  quartz,  showing  more  or  less  botryoidal  surfaces  of  an  inde- 
finable dull  greenish  color.  On  a fractured  surface  the  color  is  brown ; 
the  luster  is  resinous ; the  structure  granular,  only  occasionally  diverg- 
ing fibrous ; the  hardness  3.5 ; the  specific  gravity  of  sample  analyzed 
containing  a little  impurity,  5.88  at  19°  C.;  color  of  powder  lemon- 
yellow.  Analysis  gave  the  following  results  after  deducting  0.67  per 
cent  of  insoluble  matter : 


Molecular  ratios. 

PbO 

CuO 

FeO 

ZnO 

v2o5 

A820s 

p206  

h2o 

Cl 

Si02 

CaO 

MgO 

K20 

Na20 

C02 

57.00  j 
11.  21 
Trace. 
4. 19 
19.  79 
1.10 
| 0.19 

2. 50 
0.07 
0.80 
1. 01 
0. 04 
0.10 
0. 17 
0.  82 

98.  99 

. 2556  1 
. 1412 

J* . 4485  .4385  3.93 

. 0517  i 
. 1084  ) 

.0048  >.1145  .1115  1.00 
. 0013  j 

. 1389  1389  1.  25 

.0020 

The  low  total  is  probably  owing  to  a loss  of  zinc  during  analysis. 
Calcite  was  present  as  an  impurity,  and  as  the  C02  just  suffices  for  the 
CaO  and  MgO  these  are  rejected  in  considering  the  composition  of  the 
vanadate.  The  figures  in  the  third  column  of  molecular  ratios  are 
found  by  allowing  for  probably  admixed  vanadinite  calculated  from  the 
chlorine  found.  In  another  specimen  a qualitative  test  for  chlorine 
indicated  a greater  admixture  of  vanadinite.  As  in  the  case  of  the 
descloizite  from  Georgetown,  N.  Mex.,  previously  described,  a further 
allowance  has  perhaps  to  be  made  for  a soluble  hydrous  silicate.  There 
can  be  no  doubt  that  the  general  formula  for  the  vanadate  is  that  of 
descloizite. 

In  almost  every  respect  this  mineral  resembles,  so  far  as  the  published 
descriptions  allow  of  judging,  the  descloizite  of  Penfield,1  the  .cupro- 
descloizite  of  Rammelsberg,2  and  the  ramirite  of  de  Leon,3  perhaps 
also  the  tritochorite  of  Frenzel,4  to  the  similarity  of  which  with  his 
variety  of  descloizite  Penfield  draws  attention  in  his  paper.  Professor 
Genth’s  surmise  (1.  c.,  p.  39)  of  the  specific  identity  of  all  these  sub- 

1 Am.  Jour.  Sci.  (3),  vol.  26,  p.  361. 

* 2Monatsb.  Berl.  Acad.,  1883,  p.  1215. 

3 La  Rarairita,  nueva  espdcie  mineral,  Mexico,  1885. 

4Tschermak,s  Min.  and  Petr.  Mitth.,  vol.  3,  p.  506,  1880,  vol.  4,  p.  97, 1881. 


28 


WASHINGTON  LABORATORY. 


[BULL.  64. 


stances  seems  highly  probable.  Characteristic  of  the  present  variety 
is  the  greater  replacement  of  the  lead-zinc  vanadate — truedescloizite — 
by  the  isomorphous  lead-copper  vanadate  and  the  lessened  tendency 
toward  a fibrous  structure,  which  in  the  other  varieties  described  seems 
to  be  a decidedly  pronounced  feature.  Possibly  this  last  characteristic 
of  the  Tombstone  mineral,  if  it  be  not  accidental  in  view  of  the  few 
specimens  (three)  examined,  is  a condition  of  the  first. 

According  to  Rammelsberg,1  the  lead-copper  vanadate  corresponding 
to  the  lead-zinc  vanadate  (descloizite)  is  mottramite  or  psittacinite, 
though  it  seems  not  improbable  that  it  may  be  the  chileite  of  Dana’s 
Mineralogy.  Domeyko’s  analyses,2  which  led  Kenngott  to  ascribe  the 
above  name  to  the  Chilian  mineral,  show  a deficiency  of  2.5  and  2.8  per 
cent,  which  may  very  well  be  V205.  At  all  events,  a recalculation  of 
his  analyses  based  on  this  assumption  leads  to  a proportion  for 
PbO-f  CuO  : V205  : H20  of  nearly  4:1:1. 

In  view  of  the  well  defined  character  of  all  these  highly  cupriferous 
varieties  of  descloizite  it  would  be  well  to  designate  them  once  for  all 
by  some  distinctive  name.  Tritochorite  would  have  precedence  if  the 
substance  to  which  that  name  has  been  given  is  really  identical  with 
the  others,  but  Rammelsberg’s  cupro-descloizite  is  more  appropriate  as 
indicating  at  once  the  relationship  to  descloizite,  and  I would  suggest 
that  it  be  heneefortlf  used  for  all  cupriferous  descloizites  showing  the 
physical  characteristics  of  the  mineral  above  described. 

Note. — Since  the  foregoing  was  written  there  has  appeared  in  the 
Bull.  Soc.  Franc.  Min.,  Feb.,  1889,  p.  38,  a paper  by  F.  Pisani,  in  which 
he  gives  another  analysis  of  the  Mexican  cupro-descloizite  and  discusses 
briefly  the  relations  of  various  vanadates.  The  essential  identity  of 
all  the  above-enumerated  cupriferous  lead-zinc  vanadates,  with  the 
addition  of  another — scliaffnerite,  concerning  which  I have  been  unable 
to  find  any  further  reference  in  mineralogical  literature — is  therein 
upheld,  and  the  suggestion  of  Penfield  regarding  the  possible  identity 
of  tritoshorite  and  cupro-descloizite  is  confirmed  by  Frenzel  himself, 
who  is  quoted  as  writing  to  Professor  DesCloizeaux  that  he  had  not 
thought  it  necessary  to  consider  as  an  essential  constituent  the  two 
per  cent  of  water  which  he  had  found  in  tritochorite. 

1 Chemische  Natur  der  Mineralien,  p.  32. 

2 Ann.  d.  Mines,  IV,  vol.  14,  1848,  p.  150;  Phil.  Mag.,  Ill,  vol.  34,  1849^  p.  395. 


A NEW  METEORITE  FROM  MEXICO. 


By  J.  Edward  Whitfield. 


While  in  Mexico  during  the  summer  of  1888,  Prof.  H.  A.  Ward,  of 
Ward  and  Howell,  Rochester,  1ST.  Y.,  obtained  an  undescribed  mass  of 
meteoric  iron  weighing  33.0  kilos. 

The  meteorite  was  found  on  a peak  of  the  Sierra  de  San  Francisco, 
called  La  Bella  Roca,  in  front  of  Santiago  Papasquiaro,  in  the  State  of 
Durango.  The  date  of  its  discovery  and  the  name  of  the  finder  are 
uuknown. 

The  composition  of  the  metallic  portion  does  not  differ  materially  from 
that  of  other  meteoric  irons,  as  the  following  analysis  will  show : 


Fe 91.48 

Ni ' 7.92 

Co 0.22 

P 0.21 

S 0. 21 

C 0.06 


100. 10 

• A feature  of  the  meteorite  is  the  presence  of  large,  deep  pittings  on 
one  side $ these  are  a little  greater  in  diameter  just  below  than  imme- 
diately at  the  surface  and  each  one  has  a little  substance  left  at  the 
bottom,  which  evidently  is  the  remains  of  what  originally  filled  the 
cavities.  I succeeded  in  breaking  from  the  bottom  of  one  pitting 
material  sufficient  to  determine  its  nature.  It  proved  to  be  troilite  as 
the  analysis  will  show : 

NiS2.13,  FeS  85.27,  Fe  9.37.  • 

The  exposed  surface  of  the  troilite  was  greatly  decomposed;  this 
portion  gave  by  analysis  the  following  figures : 

NiS  2.07,  FeS  37.51,  Fe,03  37.60.  Moisture,  19.85. 

This  decomposition  gives  grounds  for  the  idea  that  the  deep  pittings 
were  formed  by  the  removal  of  troilite  nodules,  partly  while  the  mass 
was  hot  and  partly  by  the  subsequent  weathering. 


30 


WASHINGTON  LABORATORY. 


[bull,  64. 


There  are  nodules  of  troilite  throughout  the  entire  mass  of  the 
meteorite,  but  none  are  removed  so.  as  to  form  pittings,  on  any  other  part 
of  the  surface  but  the  side  which  is  supposed  to  have  been  forward. 

The  mass  is  deeply  furrowed  and  all  the  furrows  tend  away  from  the 
side  containing  the  pittings. 

Slices  of  the  meteorite,  when  etched,  show  rather  coarse  Widman- 
stattian  figures  and  also  dark  diagonal  bands  of  troilite. 

From  the  locality  in  which  this  meteorite  was  found  it  is  but  proper 
that  it  should  be  called  uLa  Bella  Boca.” 

I am  indebted  to  Messrs.  Ward  and  Howell  for  the  material  for  ex- 
amination and  the  privilege  of  description. 


DUMORTIERITE  FROM  HARLEM,  N.  Y.,  AND  CLIP,  ARIZ. 


By  J.  S.  Diller  and  J.  E.  Whitfield. 


In  1887  Dr.  R.  B.  Riggs  published  a description,  including  a chemical 
analysis,  of  u the  so-called  Harlem  iudicolite,”  which  was  regarded  as 
probably  a new  boro-silicate.  The  notice  led  to  correspondence  with 
Prof.  E.  S.  Dana,  who  identified  the  mineral  as  dumortierite,  and  kindly 
sent  us  some  of  the  original  dumortierite  from  near  Lyons,  France,  for 
comparison. 

The  physical  properties  of  the  Harlem  dumortierite  agree  very  closely 
with  those  mentioned  by  Bertrand,1  Gonnard,2  and  Darnour.3  Crystals 
are  very  rare.  An  imperfect  one4  has  been  observed  with  a(  coPoo  ) and 
m{  ocP)  equally  developed.  Both  planes  are  striated  parallel  to  the 
vertical  axis.  Indistinct  reflections  allowed  only  approximate  meas- 
urement am= 152°,  and  therefore  mm =124°.  Obtuse  terminal  planes 
rarely  observed  on  embedded  crystals. 

Cleavage  parallel  to  a is  distinctly  developed  so  that  when  the  min- 
eral is  crushed  and  examined  under  a microscope  cleavage  plates  may 
be  found  which  show  an  obtuse  bisectrix  lying  parallel  to  b(  ooPoo  ). 
Cross  fractures  occasionally  yield  basal  sections  which  may  be  made 
to  exhibit  an  acute  bisectrix.  Extinction  always  takes  place  parallel 
to  the  vertical  axis  and  the  mineral  is  evidently  rhombic.5  In  cross- 
sections  imperfect  cleavage  is  rarejy  seen  parallel  to  some  prismatic 
plane.  Polysynthetic  twinning  is  very  common  parallel  to  b as  well  as 
to  other  planes  in  the  prism  zone.  Liquid  inclusions  and  long  tubular 
cavities  parallel  to  the  vertical  axis  are  abundant.  Hardness  =7  and 
specific  gravity  slightly  above  3.265. 

The  rock  in  which  the  dumortierite  occurs  at  Harlem  is  the  pegmatoid 

1 Bull.  Soc.  Min.  d.  France,  vol.  3,  1880,  p.  171,  and  vol.  4,  1881,  p.  9. 

2 Bull.  Soc.  Min.  d.  France,  vol.  3,  1881,  p.  2. 

3 Bull.  Soc.  Min.  d.  France,  vol.  4,  1881,  p.  6. 

4 It  was  kindly  loaned  to  us  by  Mr.  R.  T.  Chamberlin,  of  New  York.  Our  thanks 
are  also  due  to  Mr.  George  F.  Kunz  for  the  material  he  so  generously  furnished  for 
this  investigation.  It  was  collected  along  Fourth  avenue  at  One  hundred  and  twen- 
tieth and  One  hundred  and  twenty-second  streets,  as  well  as  near  Fort  George,  a new 
locality  of  the  same  district. 

b My  observations,  noted  in  Mr.  Riggs’s  paper,  already  referred  to,  were  very  hastily 
made  with  imperfect  apparatus,  and  published  before  I had  an  opportunity  for  their 

revision. — J.  S.  Dillek, 


31 


32 


WASHINGTON  LABORATORY. 


[BULL.  64, 


portion  of  a biotite  gneiss.  These  coarse  vein-like  parts  are  composed 
of  quartz  with  both  red  and  colorless  orthoclase,  some  plagioclase  and 
tourmaline.  The  other  portions  of  the  rock  contain  much  biotite  and 
garnet.  The  fibers  of  dumortierite  are  sparingly  scattered  through  the 
quartz  in  the  coarse  granular  rock.  A few  were  observed  penetrating 
plagioclase.  The  thin,  thread-like  fibers  are  occasionally  so  small  as 
not  to  be  distinctly  dichroic,  but  they  are  intermingled  and  connected 
with  larger  dichroic  fibers  by  every  intermediate  gradation  in  size,  so 
that  an  observer  at  once  regards  them  all  as  the  same  mineral.  They 
sometimes  closely  resemble  the  trichitic  forms  in  granitic  quartz,  which 
Dr.  G.  W.  Hawes1  and  many  others  following  his  suggestion  regarded 
as  rutile. 

The  presence  of  tourmaline  in  the  rock  at  Harlem  was  not  at  first 
recognized.  It  is  so  intimately  associated  with  the  dumortierite  that 
they  can  not  be  easily  separated.  Their  pleochroic  phenomena,  however, 
are  so  unlike  that  they  can  be  readily  distinguished  under  a polarizing 
microscope.  The  presence  of  tourmaline  renders  the  results  of  Mr. 
Riggs’s  analysis  less  trustworthy.  By  means  of  the  Klein  solution  and 
an  electro  magnet  the  tourmaline  was  separated  from  the  dumortierite. 
The  .217  gram  of  the  latter  thus  obtained  was  analyzed  with  the  fol- 
lowing result.2  Only  the  smallest  trace  of  B203  was  observed. 

SiO-2  31.44  A1203  68.91 

Fortunately,  at  the  time  it  became  particularly  desirable  to  obtain  a 
larger  quantity  of  dumortierite  for  analysis  a collection  of  minerals  was 
sent  by  Mrs.  0.  A.  Bid  well  from  Clip,  Yuma  County,  Arizona,  to  the 
National  Museum  for  identification.  Among  them  Prof.  F.  W.  Clarke 
noticed  a blue  mineral,  which  proved  to  be  dumortierite.  It  is  finely 
fibrous  and  so  abundant  as  to  give  color  to  the  rock,  which  is  composed 
chiefly  of  granular  quartz.  A few  grains  of  magnetite  and  limonite 
are  the  only  other  minerals  intermingled  with  the  quartz  and  dumorti- 
erite, so  that  it  seems  an  easy  matter  by  means  of  a heavy  solution  and 
an  electro-magnet  to  obtain  the  latter  mineral  for  chemical  analysis. 
The  results  are  given  under  I,  below. 

These  figures  appear  to  show  the  material  analyzed  to  be  impure,  and 
it  was  thought  advisable  to  obtain  more  of  the  rock  and  endeavor  to 
separate  the  dumortierite  as  far  as  practicable  from  all  impurities. 
Mrs.  C.  A.  Bid  well  kindly  furnished  a sufficient  amount  of  much  better 
material,  in  which  the  only  mineral  associated  with  the  dumortierite 
was  quartz.  As  dumortierite  is  not  acted  upon  by  hydrofluoric  acid  ; 
the  rock,  after  being  crushed  to  small  particles,  was  digested  in  this  acid 
for  a length  of  time  sufficient  to  decompose  most  of  the  quartz.  The 
mass  was  then  washed  with  water,  dried,  and  any  quartz  that  might 
still  remain  separated  by  Thoulet’s  solution.  After  thorough  washing 

1 Mineralogy  and  Lithology  of  N.  H.,  1878,  p.  45. 

2 The  chemical  work  for  this  paper  was  done  by  Mr.  Whitfield. 


•whSfVl™]  dumortierite.  33 

the  material  was  examined  with  the  aid  of  a microscope  and  found  to 
be  free  from  gangue.  Having  been  ground  exceedingly  fine  and  dried 
at  104°  C.  for  about  three  hours,  the  mineral  was  analyzed  with  the  fol- 
lowing results  (II) : 


I. 

II. 

Si202 ....... 

31.  52  ‘ 

27.99 

A1203 

63.  66 

64.  49 

CaO 

trace. 

* 

MgO 

.52 

trace. 

Na20  

.37 

K20 

.11 

b2o3 

2. 62 

4. 95-4.  93 

p2o5 

0.  20 

Ignition 

1.34 

H20  1.72 

100. 14 

99. 35 

Analysis  II  shows  less  impurity  than  the  first  specimen  analyzed. 
These  results  indicate  either  that  dumortierite  is  not  a simple  silicate 
of  aluminum  as  stated  by  Damour;1  or  else  that  the  material  analyzed 
was  a mixture  of  dumortierite  with  some  other  compound. 

If  we  assume  the  formula  of  Damour  to  be  correct  and  estimate  all 
the  Si02  in  the  analysis  as  belonging  to  the  formula  Al8Si3018,  then 
there  will  be  left  unaccounted  for  a small  amount  of  A1203,  H20,  and 
B2G3,  and  these  are  present  in  the  proportions  represented  by  the  for- 
mula A1B306.  2H2Q.  If  this  mode  of  interpretation  be  correct,  then 
the  mineral  from  Arizona  corresponds  approximately  to  the  formula 
3Al8Si30]8.AlB306.  2H20  which  requires  Al203=65.2  percent;  Si(J2==27.6 
per  cent;  B203=5.4  per  cent;  H2Q=1.S  per  cent,  agreeing  quite 
closely  with  the  actual  analysis.  A borate  of  aluminum  corresponding 
to  the  above  formula  is,  we  believe,  not  actually  known,  and  concerning 
its  properties  nothing  can  be  predicted.  If  it  exists  it  is  certainly  re- 
markable that  it  should  withstand  the  treatment  with  hydrofluoric  acid 
which  the  dumortierite  received  during  the  process  of  purification. 

We  are  greatly  indebted  to  Mrs.  C.  A.  Bidwell  for  the  supply  of 
material  for  investigation,  which  at  the  cost  of  much  personal  labor  she 
so  liberally  furnished. 

1 Ball.  Soc.  Min.  de  France,  vol.  4,  p.  6. 


Bull.  64 3 


CHEMICAL  ACTION  BETWEEN  SOLIDS.' 


By  William  Hallock. 


In  a note  on  a new  method  of  forming  alloys  published  some  time 
ago,1 2 1 suggested  some  additional  experiments  which  I intended  to 
make,  and  I now  give  the  results  thus  far  obtained.  Unfortunately, 
other  work  prevents  my  continuing  the  investigation  at  present. 

Inasmuch  as  the  method  and  principle3  seemed  well  established 
where  metals  were  used  to  produce  alloys,  an  attempt  was  made  to 
include  some  chemical  reactions  in  the  list.  The  most  natural  cases 
were  the  freezing  mixtures  where  solid  reagents  are  used.  In  order  to 
surely  have  both  constituents  in  a decidedly  solid  state  the  experiments 
were  performed  in  a vessel  cooled  to  a temperature  of  minus  10°  or  12° 
C.,  care  being  always  taken  to  leave  the  reagents  in  the  vessel  long 
enough  for  them  to  assume  a temperature  decidedly  below  zero  Centi- 
grade. Under  these  conditions  a crystal  of  rock  salt  (NaCl)  and  a piece 
of  clean,  dry  ice  were  gently  brought  in  contact,  lying  side  by  side  on 
a watch  glass.  Of  course  the  result  was  the  solution  of  salt,  but  old 
as  this  experiment  may  be,  it  appears  here  in  a new  connection,  as  an 
example  of  the  union  of  two  solids  below  the  melting  point  of  either, 
but  above  that  of  the  product.  The  piece  of  ice  was  frozen  to  the 
glass  and  during  the  operation  the  crystal  was  drawn  several  millime- 
ters across  the  glass,  doubtless  by  capillarity,  as  the  solution  ran  out 
at  the  bottom  of  the  surface  of  contact  as  fast  as  it  formed,  the  attrac- 
tion being  sufficient  to  move  a crystal  several  grams  in  weight. 

Similar  experiments  were  performed  with  sodium  and  potassium, 
nitrate  potassium,  calcium  and  ammonium  chloride,  and  sodium  and 
potassium  hydrate,  with  a similar  result  in  all  cases.  These  are  all  well 
known  results,  but  wherein  do  they  differ  from  the  new  method  of  form- 
ing alloys  % This  question  suggests  another.  Are  the  metals  combin- 
ing to  form  an  alloy  in  the  new  way  a freezing  mixture  ? A thorough 

1 This  paper  was  read  in  part  before  the  Phil.  Soc.  of  Washington,  D.  C.,  October 
13,  1888,  and  appeared  in  full  in  the  Am.  Jour.  Sci.,  vol.  37, 1889,  p.  402. 

2 W.  Hallock,  Zeitschr.  f.  Phys.  Chem.,  vol.  2,  1888,  p.  6.  Science,  vol.  11,  1888,  p. 

265. 

3 O.  Lehmann,  Wiedemann  Ann.,  vol.  24,  1885,  p.  5,  suggested  the  theoretical  pos- 
sibility of  producing  an  alloy  in  this  way.  I had  overlooked  his  paper  until  recently. 
Mr.  Lehmann,  however,  evidently  did  not  consider  it  possible  to  fulfill  the  necessary' 
conditions  and  did  not  try  the  experiment. 

34 


HALLOCK.] 


CHEMICAL  ACTION  BETWEEN  SOLIDS. 


35 


investigation  of  the  question  would  require  more  complicated  experi- 
ments than  I had  time  to  perform.  One  test,  however,  is  very  simple, 
that  with  potassium  and  sodium. 

Into  a small  porcelain  crucible  weighing  15  grams  and  containing 
about  an  equal  weight  of  petroleum  were  placed  pieces  of  the  two 
metals,  about  3 grams  of  each.  One  junction  of  a thermo-element 
was  forced  into  the  piece  of  potassium  and  gave  its  temperature  accu- 
rately. After  the  whole  had  assumed  the  room  temperature,  clean 
faces  of  the  two  metals  were  brought  into  contact^  the  liquefaction  began, 
and  the  temperature  immediately  fell . It  required  about  two  hours  to 
complete  the  liquefaction  and  about  one  and  a half  hours  to  attain  the 
minimum  of  temperature.  No  precautions  were  taken  to  prevent  the 
calorimeter  taking  up  heat  from  its  surroundings,  and,  no  doubt,  it 
absorbed  considerable  in  the  long  time,  aud  yet  the  maximum  fall  in 
temperature  amounted  to  2.4°  C.,  very  large,  considering  the  small 
weight  of  the  reagents  compared  with  the  calorimeter.  Thus  it  appears 
that  sodium  and  potassium  are,  under  such  circumstances,  a u freezing 
mixture,”  and  analogy  at  least  would  lead  one  to  believe  that  other 
alloys  also  absorb  heat  in  their  formation;  but  future  experiment  must 
decide  the  point. 

In  the  cool  vessel  above  described  a piece  of  sodium  or  potassium  was 
placed  upon  a piece  of  dry  ice;  almost  instantly  the  reaction  commenced 
and  proceeded  vigorously.  It  is,  however,  scarcely  safe  to  consider 
this  a case  of  chemical  action  between  solids,  because  the  reaction  is 
probably  as  follows:  The  vapor  from  the  ice  attacks  the  metal,  forming 
the  hydrate  which  unites  with  other  ice,  forming  a solution,  which  is 
then  further  acted  upon  by  the  metal,  and  in  the  whole  process  heat  is 
generated  sufficient  to  raise  the  temperature  of  the  reagents  very  con- 
siderably. Perhaps  in  the  other  freezing  mixtures,  ice  and  salt,  etc.,  it 
is  the  vapor  of  the  water  or  ice  which  initiates  the  reaction. 

In  view  of  these  and  other  considerations,  the  idea  is  evident  that 
perhaps  many  substances  have  a slight  vapor  tension  at  temperatures 
considerably  below  their  melting  points,  and  are  surrounded  by  a thin 
atmosphere  of  their  own  vapor  over  their  clean  surfaces,  and  it  is  only 
necessary  to  bring  two  such  atmospheres  to  interpenetration  in  order 
to  initiate  the  reaction  which  will  then  continue,  provided  the  product 
(liquid  or  gas)  escapes  easily  and  does  not  clog  the  operation.  In  very 
many  cases  substances  are  found  to  give  oft'  a vapor  below  their  melt- 
ing point,  and  it  is  natural  to  suppose  that  there  is  a film  of  that  vapor 
over  the  surface  of  the  body,  as  there  is  a layer  of  saturated  air  over 
water.  The  mechanical  theory  of  the  composition  of  matter  lends 
plausibility  to  the  above  suggestion.  If  these  considerations  are  correct 
they  foretell  the  regelation  of  substances  like  camphor  and  ice,  without 
any  pressure  whatever.  That  loose  pieces  of  camphor  will  become 
welded  together  by  simple  contact  is  well  known.  The  operation 
appears  to  me  thus : In  an  irregular  mass  of  camphor  in  an  atmos- 


36 


WASHINGTON  LABORATORY. 


[BULL.  64. 


phere  of  camphor  vapor,  there  is  a constant  interchange  of  state  for  the 
molecules  at  the  surfaces  of  the  solid,  molecules  previously  solid  are 
getting  too  far  off  and  becoming  gas,  and  molecules  previously  gas  are 
beating  upon  the  solid  and  staying  there ; thus  the  state  of  equilibrum 
is  when,  as  a whole,  there  are  as  many  molecules  which  fly  off  and 
become  gas  as  fly  on  and  become  solid.  On  a projecting  point  of  the 
solid  the  chances  are  in  favor  of  more  flying  off  than  on;  in  a reentrant 
angle  the  reverse  is  true.  Theoretically,  then,  the  piece  ought  ultimately 
to  become  a sphere,  not  only  by  the  rounding  down  of  the  corners, 
but  by  the  building  up  of  the  flat  or  reentrant  sides.  That  the  corners 
do  round  off  all  know.  If  this  is  all  true  we  only  need  to  bring  the  two 
pieces  together  and  consider  them  as  one,  and  the  crack  between  them 
as  a reentrant  angle,  and  the  union  is  brought  about  as  above  indi- 
cated. If  in  the  above  the  word  liquid  be  substituted  for  vapor  or  gas, 
the  explanation  will  apply  to  the  regelation  of  ice  in  water  at  0°  C. 

We  may  go  even  further  and  predict  a uniting  without  actual  contact, 
and  this  prediction  has  been  experimentally  demonstrated  in  the  case 
of  ice  and  water.  A large  rough  block  of  ice  (about  15  pounds)  was 
sawed  nearly  in  two,  the  slit  washed  out  and  all  the  fine  pieces  removed. 
In  this  way  it  was  possible  to  hold  two  plane  surfaces  of  ice  parallel 
and  near  each  other  (1  t<T  2mm)  without  danger  of  actual  contact.  Into 
the  outer  edge  of  the  saw-cut  a cotton  wick  was  pressed,  thus  isolating 
the  space  between  the  faces  from  the  outside  and  preventing  any  cur- 
rents from  circulating  through  the  crack.  The  whole  block  was  then 
placed  in  water  at  zero  and  inclosed  in  non-conducting  cases  and  left 
for  twenty-five  to  thirty  hours.  This  experiment  was  tried  three  times 
and  each  time  a freezing  across  the  space  had  taken  place.  The  whole 
space  was  not  filled,  but  in  numerous  places,  notably  along  just  inside 
the  wicking  and  up  from  the  bottom  of  the  cut.  No  doubt  the  regela- 
tion would  have  gone  further  if  the  experiment  could  have  been  con- 
tinued longer.  The  melting  of  the  whole  block  puts  an  end  to  each 
experiment.  As  these  experiments  were  performed  in  summer  there  is 
scarcely  a possibility  that  the  ice  was  colder  than  0°  0. 

Inasmuch  as  there  appears  to  be  an  increasing  inclination  to  regard 
solutions  and  alloys  as  chemical  compounds,  it  seems  justifiable  to  speak 
of  the  action  according  to  the  alloy  law  as  chemical.  On  the  other 
hand,  there  are  some  cases  which  at  first  appear  as  chemical  action 
between  solids  which  upon  closer  investigation  can  be  explained  on  a 
simpler  assumption. 

For  example,  Mr.  W.  Spring,1  in  a recent  paper  on  this  subject,  cites 
three  particular  cases  as  being  chemical  action  between  solids,  the 
union  of  copper  and  sulphur,  the  reaction  between  copper  and  mercuric 
chloride,  and  between  potassium  nitrate  and  sodium  acetate. 

The  formation  of  the  sulphide  of  copper  and  other  sulphides  was  ac- 
complished by  Mr.  Spring  by  compression  of  the  elements.  But  it  is 

1 W.  Spring,  Zeitschx.  fur  phys.  Chemie,  vol.  2, 1888,  p.  536. 


HALLOCK.] 


CHEMICAL  ACTION  BETWEEN  SOLIDS. 


37 


not  even  necessary  that  the  sulphur  and  copper  be  in  contact.  I have 
made  the  sulphide  at  ordinary  temperatures  with  the  two  an  inch  apart 
and  a wad  of  cotton  in  the  tube  between  them.  It  is  simply  the  vapor 
of  sulphur  which  attacks  the  copper.  That  sulphur  gives  off  a per- 
ceptible vapor  at  ordinary  temperatures,  especially  in  vacuo,  is  a fact 
any  one  can  easily  demonstrate.  The  case  of  the  copper  and  mercuric 
chloride  is  precisely  the  same.  The  vapor  of  the  chloride  will  go 
through  a whole  tube  past  cotton  wads  and  attack  the  copper,  or  color 
potassic  iodide.  Hence  we  can  scarcely  assert  that  these  reactions  are 
between  solid  bodies.  The  reaction  between  potassium  nitrate  and 
sodium  acetate  is  equally  unconvincing.  Mr.  Spring  expected  an  in- 
terchange of  bases  and  acids  and  left  the  mixture  of  the  dry  fine 
powders  four  months  in  a desiccator  to  give  time  for  the  exchange.  On 
removing  them  from  the  desiccator  a deliquescence  was  noticeable  and 
he  therefore  concludes  that  the  interchange  had  taken  place,  since  the 
original  salts  do  not  easily  deliquesce ; but  the  product  of  the  reaction 
(potassium  acetate)  does.  It  appears  to  me  thus : The  moment  the 
powders  were  brought  to  the  air,  the  water  vapor  enters  the  operation 
and  we  have  potassium  nitrate,  water  vapor,  and  sodium  acetate,  and 
the  result  of  their  mutual  interaction  is  a solution  of  potassium  acetate 
and  sodium  nitrate.  In  fact,  if  the  dry  powdered  salts  are  stirred 
together,  in  a very  few  moments  deliquescence  begins,  showing  that 
whatever  the  reaction  it  goes  on  at  once,  and  is  a matter  of  moments 
and  not  of  months.  Thus  even  this  experiment  in  its  present  form 
does  not  convince  us  that  a chemical  exchange  took  place  before  the 
water  vapor  entered  the  reaction. 

The  question  of  chemical  action  between  solids  is  by  no  means  new, 
but  is  being  constantly  extended.  I may  say  I believe  chemical  action 
may  take  place  wherever  the  product  or  products  are  liquid  or  gaseous 
even  though  the  reagents  are  solid,  with  perhaps  the  added  condition 
that  one  or  both  the  reagents  be  soluble  in  the  liquid  produced.  If  this 
be  true  my  new  method  of  forming  alloys  is  but  a special  case  of  the 
above  general  principle.1 

1 Experiments  endeavoring  to  produce  carbon  disulphide  from  the  elements  at 
ordinary  temperatures,  are  in  hand  and  give  promise  of  positive  results.  Also,  ex- 
periments on  the  interaction  of  potassium  nitrate  and  sodium  acetate  have  been 
started  ; it  will,  however,  be  some  time  before  further  results  can  be  given. 


THE  FLOW  OF  SOLIDS:  A NOTE. 


By  William  Hallock. 


The  American  Journal  of  Science,  vol.  34,  1887,  p.  277,  contained  an 
abstract  of  my  paper  under  the  above  title,  which  appears  in  full  in 
Bulletin  55  of  the  U.  S.  Geological  Survey.  The  results  obtained  were 
so  different  from  those  of  Mr.  Spring  that  I was  led  to  a criticism  of  his 
work  and  seem  to  have  been  misunderstood.1 

The  justice  of  Mr.  Spring’s2  protest  against  a part  of  my  original 
paper  I am  glad  to  admit,  as  far  as  it  concerns  an  ill-advised  use  of 
terms,  and  a consequent  misrepresentation  of  his  views,  of  course  en- 
tirely unintentional.  Not  realizing  that  many  were  not  so  familiar  with 
Mr.  Spring’s  works  as  myself,  I neglected  in  the  brief  paper  to  give  his 
views,  and  thus  my  deductions  from  his  results  seemed  to  represent  his 
own  conclusions. 

The  object  of  my  original  investigation3  was  a solution  of  the  ques- 
tion whether  pre-sure  alone  is  capable  of  producing  true  liquefaction ; 
many  have  certainly  believed  so,  or  even  do  believe  so,  and  a few,  at 
least,  including  myself,  saw  in  Mr.  Spring’s  earlier  results  evidence  of 
such  a possibility.  I believe  that  to  produce  such  phenomena,  as  some 
recrystallizations,  and  diffusion,  an  increase  in  the  freedom  of  motion  of 
the  molecule,  an  increased  diffusibility,  i.  e.,  the  beginning  of  a lique- 
faction, is  indispensable.  Hence  i looked  upon  his  results  as  pointing 
to  a liquefaction  by  pressure.  My  own  experiments  with  the  same  sub- 
stances and  pressures  showed  the  impossibility  of  liquefying  them  by 
pressure  and  even  brought  out  an  enormous  increase  in  the  rigidity  of 
bees-wax  and  paraffin4  under  such  pressures.  In  concluding  I wished 
only  to  call  attention  to  the  difference  between  Mr.  Spring’s  results  and 
my  own,  but  unfortunately  a loose  and  abbreviated  quotation  caused 
the  misunderstanding,  which  I wish  to  explain. 

Since  obtaining  my  own  results  there  seems  to  me  little  doubt  that 
many,  at  least,  of  Mr.  Spring’s  effects  are  caused  rather  by  a motion 

1 The  following  appeared  in  Am.  Jour.  Sci.,  vol.  36,  1888,  p.  60. 

2 W.  Spring,  Am.  Jour.  Sci.,  vol.  35,  1888,  p.  78,  also  Bull,  de  PAcad.  R.  Belg.,vol.  14, 
1887,  p.  585. 

3 W.  Hallock,  Am.  Jour.  Sci.,  vol.  34, 1887,  p.  277. 

‘‘Compare  also  Ordnance  Department  Tests  of  Metals,  etc.,  1884,  Government  Print- 
ing Office,  pp.  252-254,  285-287. 

38 


HALLOCK.] 


THE  FLOW  OF  SOLIDS. 


39 


under  pressure , a kneading,  as  it  were,  and  by  the  regrinding.  The 
holders  in  which  his  compressions  were  made  were  not  tight  and  the 
most  perfect  welding1  always  took  place  at  the  surface  of  the  block,  or 
the  corners,  or  where  the  material  was  forced  into  the  cracks,  often 
even  while  the  center,  under  equal  pressure,  remained  almost  un- 
affected. My  holders  were  tight,  allowing  no  leaking  or  motion,  and 
the  substances  showed  scarcely  a trace  of  a welding  under  pressure. 
I must  therefore  reiterate  that  which  I wished  originally  to  impress, 
namely,  that  the  majority  of  Mr.  Spring’s  results  are  not  produced  by 
simple  cubic  static  pressure. 

In  the  Cases  of  chemical  action  and  the  formation  of  alloys,  I believe 
that  the  motion  under  pressure  will  be  found  to  be  the  all  important 
factor,  perhaps  just  as  stirring  assists  diffusion  to  completely  mix  two 
liquids.  Even  if  blocks  of  barium  sulphate  and  of  sodium  carbonate2 
were  brought  into  actual  chemical  contact,  I think  no  one  would  expect 
that  simple  diffusion  would  complete  the  interchange  of  bases  and  acids 
in  finite  time  so  long  as  both  substances  remained  solid  5 nor  that  a 
piece  of  copper  and  of  tin  soldered  together  would  diff  use  and  form  a 
homogeneous  bronze ; nor  would  they  expect  that  simple  cubic  static 
pressure  would  promote  these  reactions ; if  pressure  will  assist  them 
to  completion,  it  will  increase  the  diffusibility  of  solids,  increase  the 
freedom  of  motion  of  their  molecules ; that  is,  it  will  make  them  more 
like  liquids — will  begin  to  liquefy  them. 

I wish  to  refer  here  to  a new  law  I recently  proposed3  concerning  the 
formation  of  alloys,  where  the  fact  is  brought  out  that  the  melting 
point  and  liquidity  of  the  product  are  quite  as  important  as  those  of  the 
constituents  in  determining  the  possibility  of  a reaction.  Mr.  Spring4 
has  produced  Wood’s  alloy  by  compressing  the  constituents  together, 
and  quotes  Mr.  Romna5  as  having  failed  to  obtain  fine  platinum  wire 
by  electro  silver-plating  a platinum  wire,  drawing  it  down  and  dissolv- 
ing off  the  silver  in  nitric  acid,  because  the  silver  and  platinum  alloyed 
under  the  pressure  of  the  draw  plate.  Messrs.  W.  & L.  E.  Gurley,  of 
Troy,  1?.  Y.,  have  for  several  years  made  fine  platinum  wires  by  the 
well-known  Wollaston6  method  of  casting  silver  around  the  platinum  and 
treating  as  above.  In  the  note  referred  to4  I have  described  the  pro- 
duction of  Wood’s  alloy  without  pressure  at  100°  C.  of  a tin-lead  alloy 
at  190°  C.  of  the  sodium-potassium  alloy  at  ordinary  temperatures,  etc. 
Hence  it  appears  to  me  that  pressure  alone  is  the  least  important  factor 
in  the  production  of  the  effects  obtained  in  Mr.  Spring’s  investigation. 

1 W.  Spring,  Bull.  d.  PAcad.  R.  Belg. , vol.  49, 1880,  p.  352.  Phosphore  amorphe  et  seq. 

2W.  Spring,  Bull.  Soc.  Chein.,  vol.  44,  1885,  p.  166. 

3W.  Hallock,  Science,  Mar.  2,  1888,  vol.  11,  p.  100;  also  Ostwald  Zeitschr.  f.  Pliys. 
Chem.,  vol.  2,  1888. 

4 W.  Spring,  Ber.  der  deutsch.  Chem.  Gesell.,  vol.  15,  1882,  p.  595. 

6 Ibid. 

6 Ganot’s  Physics,  Atkinson,  New  York,  1883,  p.  76. 


MISCELLANEOUS  ANALYSES. 


1.  TYROLITE.1 

From  the  Mammoth  Mine,  Tintic  district,  Utah.  New  material,  very 
pure,  collected  and  analyzed  by  W.  F.  Hillebrand. 

CuO 45.08 

FeO .? r 08 

CaO .' ...  6.78 

MgO 04 

H20 17. 21 

AS2O5  ......  — . — ...... ....  — . .... .... ...  — - ....  28. 52 

S03 2.23 

Insoluble * 16 


100. 10 

2.  GADOLINITE. 

From  Llano  County,  Texas.  Analyzed  by  L.  G.  Eakins.2 

Si02 23.79 

Th02 * 58 

Fe203 96 

Ce203 2.62 

(DiLa)203 5.22 

(YEr)203 41.55 

FeO 12.42 

GIO 11. 33 

MnO trace 

CaO 74 

MgO trace 

Alkalies trace 

H20 1. 03 

P206 05 


100. 29 

In  the  rare  earths  from  this  mineral  the  absorption  spectrum  of 
didymium  was  strong,  and  that  of  erbium  was  weak.  The  molecular 
weight  of  the  oxide  (YEr)203  was  260. 


1 Compare  analyses  in  Bulletin  55,  p.  41. 

3 Compare  Hidden  & Mackintosh,  Am.  Jour.  Sci.,  Dec.,  1889. 
40 


CfiATAKP.] 


MISCELLANEOUS  ANALYSES. 


41 


3.  WARWICKITE. 

From  the  well-known  locality  at  Edenville,  Orange  County,  New 
York.  Analyzed  by  J.  E.  Whitfield.  The  material  could  not  be  com- 
pletely freed  from  an  admixture  of  spinel. 


Si 02  - 
Ti02. 
FeO.. 
AI2O3 

b2o3. 

CaO  . 
MgO. 
HoO  . 


1.16 
18. 68 
14.23 
9.  44 
18. 96 
.38 
34.41 
2.  80 


100.  06 

From  this  composition  no  simple  formula  can  be  deduced  ; but  if  we 
reject  obvious  impurities,  and  thro^out  the  alumina  in  the  form  of 
spinel,  the  residue  agrees  approximately  with  the  ratios 

Ti02  . B2O3 . 4R//0. 


This  expression  is  not  quite  satisfactory,  and  may  need  revision. 

4.  MINERALS  AND  ROCKS  FROM  MARYLAND. 

Collected  by  Dr.  G.  H.  Williams. 

Chrome  tourmaline  and  fuclisite. — Found  in  chrome  pits  a mile  west 
of  Etchison  post-office,  a little  east  of  Great  Seneca  Creek,  in  Mont- 
gomery County.  The  tourmaline  occurs  in  dark-green  needles,  with 
chromite,  and  the  mica  is  associated  with  it.  Analyses  by  T.  M.  Chat- 

ard. 


Tourmaline. 

Fuchsite. 

H20 

3.  74 

6. 77 

Si02 

36.  57 

42.21 

; b2o3 

8.  90 

F 

.06 

P2Og 

.04  • 

Ti02 

.09 

A1203 

32.  58 

34.55 

Cr203  

4.  32 

2. 03 

Fe203l  FeO 

.79 

1.03 

NiO 

.05 

MnO 

trace 

trace 

CaO 

.75 

.47 

MgO 

9.47 

3. 13 

Li20 

trace 

KajO 

2.  22 

.82 

X20 

.13 

•9. 16 

99.71 

100. 17 

42 


WASHINGTON  LABORATORY. 


[BULL.  64. 


These  minerals  are  more  fully  discussed  by  G.  H.  Williams  and  A. 
C..Gill  in  Circular  No.  75  of  the  Johns  Hopkins  University.  In  the 
same  paper  is  described  epidote  from  the  Woodstock  granite,  of  which 
the  following  analysis  has  been  made  by  Dr.  W.  F.  Hillebrand,  on  only 
0.4473  gramme  of  material: 


Si02 37.63 

Fe203(+Fe0) 15.29 

A1203 18.40 

Ti02 3.78 

MnO 31 

CaO 22.93 


MgO 31 

P2Os 44 

Ignition 2. 23 


101. 32 

Rocks  from  Baltimore  County . — Analyses  by  J.  E.  Whitfield.  A, 
pyroxenite,  Johnny  Cake  Eoad.  B,  pyroxenite,  Johnny  Cake  Eoad, 
first  stage  of  alteration.  C,  pyroxenite,  Johnny  Cake  Eoad,  second 
stage  of  alteration.  D,  smaragdite,  Dogwood  Eoad. 


♦ 

A. 

B. 

f 

C. 

1 

D. 

Si02 

50. 80 

50. 10 

51. 94 

53.22 

S03 

trace 

trace 

.19 

trace 

Cl 

.24 

.26 

.16 

.26 

P2Os 

trace 

none 

none 

AI2O3  — 

3. 40 

2.  00 

2.53 

3. 14 

Cr203  ............. 

.32 

.36 

.60 

.23 

Fe203 ............. 

1. 39 

2. 38 

2.  88 

trace 

FeO 

8.11 

8.  68 

9.  38 

7. 95 

MnO 

.17 

.29 

trace 

.11 

CaO 

12.  31 

5.06 

3.  60 

14. 44 

MgO 

22. 77 

26.  85 

25.  97 

20.  09 

Alkalies 

traces 

none 

none 

traces 

HaO 

.52 

4. 16 

2. 82 

. 98 

100. 03 

100. 14 

100.  07 

100. 42 

Titanium  was  absent  from  all  four. 


CATLETT.] 


MISCELLANEOUS  ANALYSES. 


43 


Another  pyroxenite  (E),  and  a diallage-bronzite  rock  (F),  from  the 
same  region,  were  analyzed  by  T.  M.  Chatard. 


E. 

F. 

Si02 

43.87 

53. 98 

Ti02 

.12 

.15 

p2o6 

trace 

trace 

A1203 

1.64 

1. 32 

Cr203  . — ........... 

.44 

.53 

Fe^  

8. 94 

1. 41 

FeO 

2. 60 

3. 90 

MnO 

.19 

.21 

NiO 

trace 

trace 

CaO 

6.29 

15.  47 

MgO  

27. 32 

22. 59 

Alkalies  ( AsNa2 0) . . 

.50 

undet. 

H20 

8. 72 

.92 

100.  63 

100. 48 

5.  SERPENTINE  AND  ITS  ASSOCIATES. 

From  Moriah , New  York. — Derived  from  pyroxene.  Four  analyses  by 
Charles  Catlett,  as  follows : A,  serpentine  from  the  ophiolite  of  Feed’s 
Quarry.  B,  “dolomite”  from  the  same  rock.  C,  pyroxene  from  an 
abandoned  quarry.  D,  serpentine  derived  from  the  same  pyroxene. 


A. 

B. 

C. 

D. 

Si02 

39.  96 

2. 60 

55.  36 

42.17 

A1203 ......... 

1. 07 

.09 

.22 

.30 

Fe203 

3.53 

none 

.18 

1.57 

FeO 

3. 85 

.80 

.57 

.64 

MgO 

37. 61 

2.  49 

19. 53 

41.33 

CaO 

none 

52.  38 

24. 48 

none 

C02 

none 

41.  77 

none 

MnO 

trace 

.04 

trace 

trace 

H20 

13. 65 

13.72 

99.  67 

100. 17 

100.  34 

99.  73 

Chromium  and  nickel  sought  for,  but  absent. 

Serpentine  from  the  aqueduct  shaft , New  York  City. — Analyzed  by  Mr. 


Catlett : 

Si02 . 39.92 

AL03 08 

Fe203 50 

FeO none 

MgO 42.52 

C02 1.  G4 

CaO 90 

H20  at  105° 1.36 

Ignition... 13.26 


44 


WASHINGTON  LABORATORY. 


[BULL.  64. 


From  Montville , New  Jersey. — A,  very  pale  serpentine,  somewhat  re- 
sembling deweylite  in  appearance.  B,  mineral,  resembling  actinolite.  C, 
brown  mica,  first  zone  above  pyroxene.  D,  yellowish  mica,  second  zone 
above  the  pyroxene.  E,  white  mica,  associated  with  pyroxene.  Analy- 
ses A and  B,  by  L.  G.  Eakins  ; C,  D,  and  E,  by  Charles  Catlett.  In  D 
and  E the  ferrous  oxide  was  not  separately  estimated  for  want  of  suf- 
ficient material. 


Associates  of  serpentine  from  Easton , Pennsylvania. — A,  vermiculite, 
analyzed  by  C.  Catlett;  B,  tremolite;  C,  so-called  “nephrite.”  Analy- 
ses B and  C by  L.  G.  Eakins. 


A. 

B. 

C. 

Si02 

42.  21 

58.  27 

60.  29 

A1203  

9.37 

.33 

20.  83 

Fe203  

.68 

trace 

trace 

FeO 

none 

MnO 

none 

.08 

CaO 

none 

11.  90 

. 16 

MgO 

34.  80 

25.93 

6. 44 

Na20 

1.  25 

1. 25 

1.97 

k2o 

1.34 

.42 

8.  41 

H20 

10.70 

1.22 

1.13 

100. 35 

99. 40 

99.  23 

All  of  the  foregoing  minerals  were  collected  by  Mr.  G.  P.  Merrill. 


A. 

B. 

C. 

H20 

14.  73 

1. 17 

5.07 

C02 

1 .30 

Si02 

40.  64 

43. 31 

39. 38 

A1203.  

2.  74 

17.41 

15.  92 

Fe203 

.81 

.71 

.71, 

.80$ 

FeO 

.28 

. 59 

MnO 

trace 

. 14 

trace 

CaO 

trace 

12.84 

.28 

MgO 

40.93 

19.  39 

26. 85 

Na20 

2.23 

.62 

K20 

1. 36 

9. 84 

F 

.62 

Less  O.. 

100. 13 

99. 15 

100.  39 
. 26 

100.13 

D. 

E. 

10. 88 

10.  20 

1.  80 

32. 52 

39. 14 

18. 14 

15. 70 

2.30 

1.68 

trace 

trace 

1. 44 

5.  24 

29.26 

25.  44 

1. 38 

.64 

2. 78 

2.06 

10C.  50 

100. 10 

CHATARD.] 


MISCELLANEOUS  ANALYSES. 


45 


6.  GEYSERITES  FROM  ROTORUA,  NEW  ZEALAND. 

Received  from  the  museum  at  Auckland.  Analyzed  by  J.  E.  Whit- 
field for  comparison  with  the  geyserites  of  the  Yellowstone  Park,  which 
they  closely  resemble.  Three  samples  : 


1. 

2. 

3. 

Si02 

92.47 

90.  28 

74.  63 

A1203 

2.  54 

3.  00 

15.  59 

CaO 

.79 

.44 

1.00 

MgO 

• 15  ■ 

trace 

trace 

Ha20 

.30 

K20 

1.  02 

Ignition 

3. 99 

6. 24 

7.43 

99.94 

99.  96 

99.  97 

7.  MISCELLANEOUS  ROCKS. 

Sandstone  from  Buena  Vista , Ohio. — A yellowish  building  stone.  Par- 
tial analysis  by  F.  W.  Clarke. 


Moisture 2.51 

SiO-2 88.27 

Al.2O3-fFe.2O3 9.09 

MgO trace 


99. 87 

Insoluble  in  HC1 96.47 

Soluble  FezOa 77 


Sandstone  from  near  Portsmouth , Ohio. — The  “ Peebles-Henley  77  or 
“Otway’7  building  stone.  Three  samples,  analyzed  by  T.  M.  Chatard. 
In  B and  C the  iron  was  mainly  ferrous,  though  weighed  as  Fe203. 


i A. 

B. 

C. 

Ignition 

1.08 

1.46 

1.95 

Insoluble  in  HC1 

98.  31 

97.  20 

95. 83 

Soluble 

.61 

1.40 

2.  42 

. 

100.  00 

100. 06 

100. 20 

Soluble  Fe^ 

.61 

i7oT 

1.6  5~ 

Soluble  CaO 

trace 

.36 

.77 

! Soluble  MgO 

trace 

little 

trace 

46 


WASHINGTON  LABORATORY. 


[BULL.  64. 


Limestone  from  Silverdale , Kansas. — Analyzed  by  Charles  Catlett. 

5. 27 
1.07 
.71 
.32 
50. 36 
.56 
.20 
.10 
40. 34 
.07 
.06 
.78 


99. 84 

Metamorphic  rock  from  Marion , Kentucky. — Analyzed  by  L.  G.  Eak- 


34. 50 
14. 37 
2. 85 
4.46 
11.43 
21.81 
1.50 
. 51 
7. 14 
.77 
.60 
.21 


100. 15 

From  Pigeon  Point , Michigan. — Analyses  by  L.  G.  Eakius.  A,  red  por- 
phyry from  Brick  Island,  Lake  Superior,  near  Pigeon  Point.  B,  green 
mottlings  from  Pigeon  Point.  Van  Hise’s  rock,  No.  11908. 


A. 

B. 

sl02  — ....... 

73.70 

83.27 

Ti02 

.12 

trace 

AI2O3 

12. 87 

7. 81 

F62O3 

3. 76 

1.99 

FeO 

.31 

1. 81 

MnO 

.07 



CaO 

.14 

.20 

MgO 

.11 

1. 59 

K20 

4.  56 

1.11 

Na20 

3.63 

.19 

H20 

.57 

2. 32 

P2Of 

trace 

trace 

99.  84 

100.  29 

Si02  • - 
A1203 . 
Fe203*. 
FeO.. . 
CaO  .. 
MgO. . 
K20.  . 
Na20  . 

h2o.. 

F2O5 . . 

S03... 

co2... 


Si02 . 
A1203 
Fe203 
FeO  . 
CaO. 
MgO. 
Na20. 
K20  . 

co2.. 

so3.. 

p2o5. 

h2o. 


E AKINS.] 


MISCELLANEOUS  ANALYSES. 


47 


Diabase , Penokee- Gogebic  Range , Michigan . — Analyses  by.  T.  M.  Cha- 
tard.  A,  from  near  SE.  corner  of  Sec.  13,  T.  47  N.,  R.46  W.  B,  altered 
diabase,  same  locality.  0,  altered  diabase,  Aurora  Mine,  NE.  J ot  S W. 
J Sec.,  T.  47  N.,  R.  47  W.  D,  feldspar  separated  from  A. 


A. 

B. 

C. 

D. 

H20,  at  105° 

.15 

3.12 

.29 

\ 1 1 Q 

H20,  at  red  heat 

2.34 

8.25 

13.  54 

/ i. 

C02 

.38 

1.89 

.38 

1.  89 

p2o5 - 

. 13 

. 16 

. 14 

Si02  

47.  90 

46. 85 

41.60 

51.18 

Ti02 

.82 

1. 12 

3.  79 

A1203 

15.60 

22.  62 

37. 20 

27. 00 

Fe203  

3.69 

5.12 

3.21 

3. 19 

Cr203  

trace 

FeO 

8. 41 

1.  58 

: 30 

undet. 

NiO 

. 10 

. 08 

MnO 

.17 

2.  54 

.08 

.17 

BaO 

.05 

. 10 

trace 

CaO 

9. 99 

1.  25 

.23 

11.70 

MgO 

8.11 

2.01 

.02 

1. 92 

k2o 

.23 

2. 66 

.41 

NajO 

2. 05 

.80 

.07 

3. 48 

100. 12 

100. 15 

100.  85 

100.  24 

Penokee-  Gogebic  rocks  from  Wisconsin. — A,  B,  0,  three  slates,  analyzed 
by  L.  G.  Eakins.  A,  from  Sec.  6,  T.  45  N.,  R.  2 E.  B,  from  Sec.  1,  T. 
45  N.,  R.  1 E.  0,  from  Sec.  4,  T.  44  N.,  R.  2 W. 


A. 

B. 

C. 

Si02  .............. 

53.44 

59.  73 

52.  58 

A1203 

19.  62 

22.  78 

20.  76 

Fe203 

11.  38 

.11 

12. 17 

FeO 

5. 35 

5. 98 

4.  08 

MnO 

trace 

.09 

.21 

CaO 

.42 

.53 

.30 

MgO 

1.58 

2.  94 

1.  33 

K20 

1.73 

3. 48 

4.  87 

NaiO 

2. 61 

1.41 

.37 

Li20 

trace 

trace 

H20 

4.07 

3.  28 

3. 43 

P2Os 

trace 

100. 20 

100.  33 

100.  10 

48 


WASHINGTON  LABORATORY. 


| BULL.  64. 


D,  E,  F,  three  feldspars,  analyzed  by  T.  M.  Chatard.  D,  from  gabbro, 
center  of  Sec.  14,  T.  4£  N.,  R.  4 W.  E,  F,  from  olivine  diabase,  NE.  J 
Sec.  13,  T.  45  N.,  R.  1 W. 


D. 

E. 

F. 

H20,  at  105° 

.03 

.13 

H2O,  at  red  lieat  . . 

.54 

5 -9o ! 

.64 

Si02 

51.99  j 

61.  65 

56.15 

ai2o3 

29.32  ! 

19.91 

26.  05 

F e203  — 

1.23  j 

2.28 

1.  98 

FeO 

undet. ! 

undet. 

undet. 

MnO 

trace  j 

. trace 

.13 

CaO 

12.  GO  i 

4. 12 

8.70 

AT  crO  ..... 

.63  1 

.61 

. 54 

k2o 

.28 ; 

5.  72 

1.  56 

Na^O 

! 2.91  ! 

4. 74 

i 4.79 

j 99.53 

99.98 

100.67 

Eruptive  rock  from  four  miles  southwest  of  Hot  Springs , Arkansas. — , 
Analyzed  by  L.  G.  Eakins. 


SiO,  . 
Ti02  . 

ai2o3. 

Fe203 
FeO  . 
CaO  . 
MgO. 
K20. 
Na,0. 
H20  . 
C02  . 
P2O,. 


36. 40 
.42 
12. 94 
8.27 
4.59 
14.  46 
11.44 
3.01 
.§7 
2.  36 
3. 94 
1.04 


99. 84 


Recent  lava  from  two  miles  south  of  Mount  Trumbull , Arizona. — - 
Analyzed  by  L.  G.  Eakins. 


Si02  . 
Ti02  . 
A1203 
Fe203 
FeO  . 
M11O. 
CaO. 
MgO. 
K20  . 
Na20 
H20- 
P2O,. 


45. 30 
2. 66 
14.95 
1.98 
9.32 
trace 
8. 87 
8.29 

1.27 

4.27 
.85 

2.23 


99. 99 


Bakins.]  MISCELLANEOUS  ANALYSES.  49 

Eruptive  rock  from  Castle  Mountain , Montana. — Analyzed  by  L.  G. 

Eakins. 

Si02  44. 66 

Ti02 1.02 

A1303 - 12.12 

F 62O3 5.81 

FeO 3.20 

MnO 21 

CaO 8. 14 

MgO 8.  77 

K20 : 2.75 

Na20 - 4.47 

H20 4. 33 

C02 2.19 

P205  2. 02 


99. 69 

Rocks  from  Northern  California . — Collected  by  J.  S.  Diller.  A, 
porphyritic  rocks  from  Shasta  County;  analyzed  by  J.  E.  Whitfield, 
east  fork  of  Clear  Creek,  nine  miles  from  French  Gulch.  B,  Smith’s 
Gulch,  six  miles  up  Clear  Creek  from  French  Gulch. 


A. 

B. 

Si02 

66. 30 

64.24 

Ti02 

trace 

.76 

S03 

.28 

.22 

Cl 

none 

.25 

P2O5 

.15 

.08 

ai2o3 

17.55 

18.  67 

F e203 

2.19 

1.40 

FeO 

.55 

1.96 

MnO 

trace 

trace 

CaO 

3. 12 

4.11 

MgO 

.97 

1.48 

NTa20 

5. 15 

4. 14 

k2o 

2. 45 

1.71 

H20 

1.25 

1.18 

99.  96 

100. 20 

Bull.  64 4 


W 


50 


WASHINGTON  LABORATORY. 


(bull.  64. 


C,  D,  two  rocks  from  tliree-fourtks  of  a mile  below  John  Allen’s,  Dry 
Creek,  Shasta  County.  E,  from  John  Allen’s.  F,  from  two  and  one-half 
miles  above  John  Allen’s.  Analyses  by  Whitfield. 


G,  eruptive  rock,  Great  Bend  of  Pit  River.  H,  black  obsidian,  Medi- 
cine Lake,  Modoc  County;  analyses  by  L.  G.  Eakins. 


Gr. 

H. 

Si02 

44. 77 

73.  51 

Ti02 

. 53 

p206. 

.72 

.04 

A1203 

17.  82 

14.  42 

F e203 ......... 

5.  05 

.46 ; 

FeO 

6. 95 

1.49  | 

M11O 

trace 

trace  | 

CaO 

10. 36 

1.26  | 

MgO 

8.22 

.33  | 

Na20 

2. 13 

4.03  ! 

K20 

.92 

4.  29 

H20 

2.64 

.40  : 

100. 11 

100.23  j 

C. 

D. 

E. 

F. 

Si02  .......... 

59. 10 

61.  60 

54.  55 

60.74 

Ti02 

.70 

trace 

trace 

.86 

S03 

trace 

.27 

.10 

.40 

Cl 

trace 

trace 

.12 

trace 

P2O5 

trace 

.08 

.10 

trace 

A1203 

14.02 

12. 15 

10.64 

10.25 

Fe203 

3. 16 

2.  09 

1.59 

4.31 

FeO 

1.42 

3. 30 

1. 16 

6.21 

MnO 

trace 

trace 

1.  53 

trace  j 

CaO 

9.35 

6.  92 

14.  30 

4.97  | 

MgO  

1. 72 

2. 33 

1.29 

3.69 

Na20 

2. 21 

2. 16 

2.  60 

1.  83 

K20 

1.49 

1.41 

1.68 

.52 

C02 

4.  65 

5. 05 

9.  05 

2.  29 

H20  

2.  63 

3. 10 

1. 60 

4.  36 

100.  45 

100.  46 

100.  31 

100. 43 

CATLETT.] 


MISCELLANEOUS  ANALYSES, 


51 


8.  SOILS  AND  CLAYS. 

A,  kaolin  from  Talladega,  Alabama.  B,  clay  from  Richfield  Springs, 
New  York;  partial  analysis.  C,  D,  two  clays  from  Northumberland 
County,  Pennsylvania;  analyses  by  Charles  Catlett. 


A. 

B. 

C. 

D. 

H20,  at  120° 

H20,  at  red  heat 

5.02 
13. 48 

00 

to 

| 6.28 

j 6.87 

Si02  

43. 21 

49.  65 

65.  97 

59. 16 

Al203 

37.27 

|23.  82 

20.37 

18.  68 

F e203 — .. 

trace 

2. 75 

10. 32 

CaO 

.11 

6. 48 

.64 

.52 

MgO 

.30 

trace 

.52 

.67 

K20 

.28 

undet. 

3. 32 

3.  35 

Na20 

.40 

undet. 

.05 

.11 

99. 87 

96. 13 

99.  90 

99.  €8 

E,  F,  G,  H,  adobe  soils.  E,  from  Santa  Fe,  New  Mexico.  F,  Fort 
Wingate,  New  Mexico.  G,  Humboldt  City,  Nevada.  H,  Salt  Lake 
City,  Utah.  Analyses  by  L.  G.  Eakins. 


E. 

F. 

G. 

H. 

Si02  ...... .......... 

66. 69 

26. 67 

44.  64 

19.24 

A1203 

14. 16 

.91 

13.19 

3.  26 

Fe203 

4.38 

.64 

5. 12 

1.  09 

MnO 

.09 

trace 

.13 

trace 

CaO 

2. 49 

36.40 

13.91 

38. 94 

MgO 

1. 28 

.51 

2.  96 

2. 75 

k2o 

1. 21 

trace 

1. 71 

trace 

Na^ 

.67 

trace 

. 59 

trace 

C02 

.77 

25.  84 

8.  55 

29. 57 

p2o6 

.29 

.75 

.94 

.23 

S03 

.41 

.82 

.'64 

.53 

Cl ? 

.34 

.07 

.14 

.11 

h2o 

4.  94 

2. 26 

3. 89 

1.67 

Organic  matter 

2.00 

5. 10 

3.43 

2.  96 

99. 72 

99.  97 

99. 84 

100. 35 

9.  ORES  OF  IRON  AND  MANGANESE. 


Manganese  ore,  Powell’s  Fort,  east  end  of  Massanutten  Mountain. 
Warren  County,  Virginia.  Analysis  by  Charles  Catlett. 


Si02 
Fe.. 
Mn  . 
P... 
S... 


9. 20 
3.  07 
48.  .^9 
.349 

,12 


52 


WASHINGTON  LABORATORY. 


[bull.  61 


Iron  and  manganese  ores,  Montebello,  Nelson  County,  Yirginia. 
Analyses  by  Catlett. 


Iron. 

Manganese. 

Si02 

16. 47 

1.68 

Fe 

51. 10 

2.  60 

Mn 

.65 

46. 99 

P 

.152 

.464 

S 

.11 

.21 

Ores  from  Rockbridge  County,  Yirginia;  analyzed  by  T.  M.  Chatard. 
A,  top  of  hill  above  Hart’s  Bottom,  one  and  three-fourths  miles  southwest 
of  Green  Forest  Station,  near  Lockland  Station.  B,  Moorman  Quarry, 
Green  Forest.  C,  new  opening,  No.  2,  Buena  Yista.  D,  opening,  No.  3, 
40-foot  vein,  Buena  Yista.  E,  Chalk  Mine  Branch.  F,  Old  Colonial 
opening,  Buena  Yista. 


A. 

B. 

C. 

D. 

E. 

F. 

H20,  105° 

.72 

.15 

.39 

.60 

.45 

.48 

Insoluble 

20. 40 

13.47 

22.55 

16. 60 

8. 05 

5. 43 

Soluble  AI2O3 . - ■ 

1.  67 

.37 

1.  81 

.46 

Ti02  

. 16 

Fe203 

3.11 

76. 19 

66. 58 

71. 16 

78.24 

82. 15 

NiO 

. 27 

MnO 

53.91 

.45 

.22 

.11 

.66 

.19 

BaO 

.23 

S03 

.32 

.14 

.09 

.37 

trace 

.08 

P2O5 

.50 

.26 

.42 

.50 

.88 

1.04 

Fe 

2.18 

53. 33 

46.  60 

49.  81 

54.  76 

57.50 

Mn 

41.  59 

P 

.22 

.11 

.18 

.22 

.38 

.45 

S 

.12 

. 06 

.03 

.14 

.02 

Two  manganese  ores.  Cripple  Creek,  eight  miles  from  Wytheville, 
Yirginia.  Analyses  by  C.  Catlett. 


1. 

} 

2. 

SiOa 

47.  30 

27.86 

Fe 

2. 72 

3.  61 

Mn 

24.  85 

32. 55 

P 

.05 

.097 

S 

trace 

.030 

Iron  ore  from  Shanghai,  West  Yirginia.  Analyzed  by  C.  Catlett. 


Si02 
Fe  . 
Mu  . 


45.24 
26.  02 
.43 


CATLETT.! 


MISCELLANEOUS  ANALYSES. 


53 


Two  iron  ores  from  Kentucky ; analyzed  by  J.  E.  Whitfield.  A, 
Cloverport  Road,  two  miles  north  of  Fordsville,  Ohio  County.  B,  north 
slope  of  Pine  Mountain,  three  miles  east  of  Pineville,  Bell  County. 


A. 

B. 

Si02  .............. 

35. 67 

17. 28 

Ti02 

trace 

trace 

Cl 

trace 

so3 

.42 

.40 

p206  

1.42 

trace 

ai2o3 

6. 15 

.35 

F ©203 

42.  31 

68. 24 

FeO 

.35 

trace 

MnO 

.84 

.95 

CaO 

1.90 

.83 

MgO 

1. 07 

.92 

Ignition 

9.  69 

11. 60 

99. 82 

100. 57 

Fe 

29.  86 

47.77 

p 

. 71 

s 

.16 

.15 

Iron  ore.  Douglass  Mine,  Clinton  Horizon,  one  mile  west  of  Big 
Creek  Gap,  Campbell  County,  Tennessee.  Analyzed  by  W.  F.  Hille- 
brand. 


Si02 

Fe.. 

Mn. 


10. 51 
54. 29 
.20 


P 355 

S 043 


Two  iron  ores  ; analyzed  by  C.  Catlett.  A,  from  Edgefield  County, 
South  Carolina.  B,  north  part  of  Howard  County,  Arkansas. 


A. 

B. 

Si02  ............ 

9. 40 

28.10 

Fe 

52.  40 

29.  57 

Mn 

trace 

2. 19 

P 

.664 

.483 

S 

.08 

.04 

54 


WASHINGTON  LABORATORY. 


[RULL.  64. 


10.  COAL  AND  COKE. 

Three  coals.  Raccoon  Fork  of  Cabin  Creek,  Kanawha  County,  West 
Virginia.  Analyzed  by  E.  L.  Howard. 


1. 

2. 

3. 

Moisture 

1.  93 

2. 15 

1.67 

Volatile  matter . . . 

37.  09 

23.  95 

41.  36 

Fixed  carbon 

57.  90 

61.  85 

53. 22 

Ash 

3. 08 

12.  05 

3.  75 

100.00 

100. 00 

100. 00 

Sulphur 

.62 

.46 

.80 

Ash 

dirty  white 

light  gray 

reddish 

Coal  and  coke.  Davis  Mine  No.  1,  near  North  Fork  of  Blackwater, 
Tucker  County,  West  Virginia.  Analyzed  by  Charles  Catlett. 


Coal. 

Coke. 

Moisture 

.80 

.18 

Volatile., matter  . . . 

26. 84 

1.49 

Fixed  carbon 

67. 18 

90. 60 

Ash 

5.18 

7.  73 

100.  00 

100.  00 

Sulphur 

1.68 

.771 

Ash 

very  light  red 

light  red 

Five  coals.  Campbell  County,  Tennessee ; A,  B,  C analyzed  by  W.  F. 
Hillebrand;  D,  E by  Charles  Catlett.  A,  Douglass  Bank,  Middle  Fork 
of  Big  Creek,  one  and  one  half  miles  from  Gap,  lower  coal-measures. 
B,  Walnut  Mountain,  head  of  Hickory  Creek,  Clear  Fork  of  Cumber- 
land River,  2,850  feet  above  sea-level,  upper  coal-measures.  C,  Middle 
Fork  of  Big  Creek,  lower  coal-measures.  D,  East  Fork  of  Big  Creek. 
E,  Middle  Fork  of  Big  Creek,  three  miles  from  Big  Creek  Gap. 


A. 

B. 

C. 

D. 

E. 

Moisture 

1.49 

2.  95 

1.11 

1.70 

7.  60 

Volatile  matter... 

39. 00 

38. 51 

35. 59 

39.41 

34. 89 

Fixed  carbon 

53.  30 

55.42 

23. 99 

55. 36 

53. 14 

Ash 

6.  21 

3. 12 

39.31 

3. 53 

4. 37 

100. 00 

100. 00 

100. 00 

100. 00 

100. 00 

S 

1. 53 

.87 

2. 78 

1. 07 

.64 

P 

.041 

A rough  test  on  C showed  that  one  ton  of  coal  should  yield  40,000 
cubic  feet  of  gas. 


BAKINS.]  MISCELLANEOUS  ANALYSES.  55 

Also  two  cokes,  analyzed  by  C.  Catlett.  F,  Walnut  Mountain,  Hickory 
Creek.  G,  from  Sharp  coal,  Left  Fork  of  Big  Creek. 


F. 

G. 

Moisture 

.20 

.50 

Volatile  matter... 

2.01 

1.  95 

Fixed  carbon 

85.  56 

91.71 

Asb 

12.  23 

5.84 

100.  00 

100.00 

S 

.886 

.705 

P 

.040 

undet. 

Thirty-two  coals  from  Gunnison  County,  Colorado.  Collected  by  G.  H. 
Eldridge,  and  analyzed  by  L.  G.  Eakins. 

From  Anthracite  Creek  Mines. 


Moisture 3. 95 

Volatile  matter 4. 65  ' 

Fixed  carbon 82.  34 

Ash 9.06 


100.  00 


.63 
.07 

Specific  gravity 1.644 — 24.4° 

Ash,  light  red $ no  coke. 

From  Green  Mountain,  Denver  Beds. 


Moisture 8.91 

Volatile  matter 46.16 

Fixed  carbon 44.46 

Ash 47 


100.  00 


.47 

1.  381—22.  5° 


S 

Specific  gravity 

Ash,  light  red ; coke  moderately  coherent. 


S 

P.  in  ash 


56 


WASHINGTON  LABORATORY. 


[BUHL.  64. 


From  Ohio  Creek  Mines,  Nos.  1 to  11. 


1. 

2. 

3. 

4. 

5. 

Moisture 

7.39 

8.  46 

8. 26 

1.61 

1.  34 

Volatile  matter 

39.43 

39. 01 

39. 96 

13. 05 

30.  25 

Fixed  carbon 

47.83 

46.  68 

46. 36 

80. 29 

62.  38 

Ash 

5. 35 

5. 85 

5.42 

5.  05 

6.03 

100. 00 

100. 00 

100. 00 

100.  00 

100. 00 

s 

1.47 

.76 

.68 

.59 

.44 

P.  in  ash  

.06 

.07 

Specific  gravity 

1.328,  23° 

1.334,  21.6° 

1.331,  25° 

1.407,  23° 

1.325,  22o 

Ash 

reddish  gray .... 

light  rod 

light  red 

red  

red 

Coke 

fairly  coherent 

cokes  slightly 

cokes  slightly. 

none 

firm,  solid. 

6. 

7. 

8. 

9. 

10. 

11. 

Moisture 

6. 28 

6. 37 

6.  39 

1.07 

1. 23 

.81 

Volatile  matter. 

40.  92 

38.  06 

39. 26 

26. 22 

26. 65 

9. 96 

Fixed  carbon  . . . 

46.  35 

49. 75 

48.41 

68.  36 

68. 27 

82.  33 

Ash 

6.  45 

5.  82 

5. 94 

4.  35 

3. 85 

6.  90 

100. 00 

100.  00 

100. 00 

100.  00 

100. 00 

100. 00 

S 

.47 

.46 

.46 

.60 

.61 

1.  06 

P.  in  ash 

.03 

.05 

Specific  gravity. 

1.324,  210 

„ 1.345,  21.6° 

1.337,  23° 

1.319,  22° 

1.317,  22° 

1.426,  23.8° 

Ash 

reddish  yellow 

reddish  yellow . . 

red 

red 

red 

pinkish  gray. 

Coke 

fair 

slightly  coherent 

fair 

fair 

fair 

none 

From  Slate  Creek  Mines,  Nos.  12  to  21. 


12. 

13. 

14 

15. 

16. 

Moisture 

1. 29 

1.36 

1.86 

1. 35 

1.30 

Volatile  matter 

7. 92 

7. 53 

6.  68 

6.  59 

7.  55 

Fixed  carbon 

85.  71 

85.49 

86.  25 

72.  34 

80.  44 

Ash 

5. 08 

5.62 

5.21 

19.72 

10.71 

100.  00 

100.00 

100.  00 

100.  00 

100. 00 

S 

.67 

.54 

.69 

.66 

.58 

P.  in  ash 

.4)5 

. 03 

.32 

Specific  gravity 

1.428, 23.4° 

1.440, 21.8° 

1.465, 26.40 

1.481, 22.2° 

1.502, 22.8° 

Ash.. 

red 

red 

red _ 

prrav  ...... 

light  red . . 

Coke 

non© ...... 

non© 

non© 

non© 

non© 

17. 

18. 

19. 

20. 

21. 

Moisture 

1.58 

1.  22 

1.27 

.92 

.81 

Volatile  matter 

6.  70 

8.46 

7.  99 

14. 19 

13.40 

Fixed  carbon 

87. 46 

84.  20 

87.24 

81. 29 

81.26 

Ash 

4.26 

6. 12 

3.  50 

3.  60 

4.53 

100.  00 

100. 00 

100. 00 

100.00 

100. 00 

S 

.58 

. 76 

.^2 

• 52 

.51 

P.  in  ash 

non© 

Specific  gravity. .. 

1.455,  22.8° 

1.409, 22° 

1.409, 23.3° 

1.359,  20.4° 

1.371, 20  8° 

A ah  - 

red 

red  

red 

light  red 

red  

Coke.... 

non© 

none 

non© 

cokes  slightly. 

cokes  slightly. 

CEATAED.] 


MISCELLANEOUS  ANALYSES, 


57 


From  Crested  Butte  Mines,  Nos.  22  to  30. 


22. 

23. 

24. 

25. 

Moisture  

1. 36 

1.47 

1.  94 

2.  36 

Volatile  matter. . 

37. 12 

38. 09 

41.07 

40. 82 

Fixed  carbon 

57.73 

56. 68 

51.48 

50.49 

Ash 

3.  79 

3. 76 

5.  51 

6.  33 

100. 00 

100. 00 

100.  00 

100. 00 

S 

49 

,47 

.63 

1.04 

07 

trace  

Specific  gravity 

1.288,  22.6° 

1.276,  21° 

1.311,  21.1° 

1.332,  22° 

A ah 

licrht  red 

licrht  _ . 

red 

red 

flotft 

trend 

creed  _ 

good 

good 

26. 

27. 

28. 

29. 

30. 

Moisture 

1. 88 

2.  09 

1.76 

3. 95 

4. 83 

Volatile  matter. 

39.  51 

41.74 

42. 00 

37. 17 

37. 86 

Fixed  carbon  ... 

54.  42 

52.07 

51.  97 

52.  34 

51.  65 

Ash 

4. 19 

4. 10 

4. 27 

6. 54 

5.  66 

100. 00 

100. 00 

100. 00 

100.  00 

100. 00 

s 

.63 

.65 

.75 

.42 

.68 

P.  in  ash 

trace  

Specific  gravity. 

1.288,  24.8° 

1.289,  26.6° 

1.286,  20° 

1.328,  22.4° 

1.349,  21.20 

A ah 

red 

red 

light  red . . 

red 

red 

Celt  a. 

good,  solid 

(rend 

trend 

hn/rrl  cnnmuct. 

fair 

11.  ANALYSES  OF  WATERS. 

Analyzed  by  T.  M.  Chatard.  A,  from  the  Murray  Well,  one  mile 
north  of  Frankfort,  Kentucky.  Slight  odor  of  H2S.  Specific  gravity, 
.99984,  22°. 


Found, 
grammes 
per  liter. 

Per  cent, 
of  total 
contents. 

Combina- 

tion. 

Rif)2 

.0096 

.61 

C02 

.0172 

Fe 

.0014 

.08 

nh3 

.0015 

Ca 

.0213 

1.35 

KC1 

.0396 

Sr? 

.0122 

. 71 

NaCl  

.8287 

Mg 

.0189 

1.20 

Na2S04  . .. 

.2770 

K 

.0207 

1.31 

FaH2C2Oc 

. 0045 

Na 

.4604 

29. 35 

CaH2n2Oc  . . 

. 0862 

Li 

trace 

SrTTjjftjOg? 

.0269 

SO* 

.1873 

11.93 

MvTToCoO^ 

.1150 



Cl 

.5218 

33.  23 

NaHCOs 

.1639 

COJ 

.2929 

18. 74 

Si02  ... 

.0096 

C02,  free 

.0172 

1.09 

NHS 

.0015 

.09 

H,  in  bicarbonates 

.0049 

.31 

1. 5701 

100.  00 

1.  5701 

The  strontium  is  doubtful,  and  may  be  only  a strong  trace. 


58 


WASHINGTON  LABORATORY, 


[BULL.  64; 


B,  spring  water  from  Mountain  City,  Tennessee.  Statement  like  the 
preceding. 


Found. 

Per  cent, 
of  total. 

Combina- 

tion. 

. 0219 

21. 26 

Si02 

. 0219 

Fe 

.0008 

.78 

FeH2C206 

.0026 

A1  

trace 

CaH2C206 

.0448 

Ca  

.0116 

11. 26 

MjrHoC„0, 

.0110 

Mg 

.0018 

1. 75 

b * ^ •*••■**• 

CaS04 

.0018 

Na 

.0046 

4.  47 

Na2S04  

.0142 

K 

.0032 

3. 11 

k2so4 

.0042 

Cl 

.0012 

1. 16 

KC1 

.0025 

so4 

.0132 

12.  81 

COg 

.0440 

42. 72 

H,  bicarbonates  .. 

.0007 

.68 

.1030 

100. 00 

.1030 

C,  the  Grace  Spring,  seven  miles  north  of  Mountain  City,  Tennessee, 
on  the  road  to  Abingdon,  Virginia,  near  Laurel  Bloomery  post-office. 
Specific  gravity,  1.00038,  18.5°. 


Found. 

Per  cent, 
of  total. 

Combina- 

tion. 

SiOj 

.0125 

1. 09 

Si02 

.0125 

Fe 

trace 

KC1 

.0023 

Ca  

.2334 

20. 31 

KoSOjj 

.0075 

Mg 

.0580 

5. 05 

Na2S04 

.0145 

K 

. 0046 

.40 

MgS04 

. 2900 

Na 

.0047 

.41 

CaS04 

.6429 

Cl 

.0011 

.09 

CaTLjCoOg  

. 1794 

so4 

.6997 

60. 89 

COg 

.1329 

11.57 

H,  bicarbonates. . . 

.0022 

.19 

1. 1491 

100. 00 

1. 1491 

chatard.]  MISCELLANEOUS  ANALYSES.  59 

D,  drinking  water,  Savannah,  Georgia.  Stated  in  grammes  per  liter. 


Found. 

Combina- 

tion. 

Suspended  matter  (organic) . . . 

.0020 

Suspended  matter 

.0025 

Suspended  matter  (inorganic). 

.0005 

Si02 

.0624 

Si02 

.0624 

-A.I0O5.  FcoOq 

.0006 

AlA,  FesO* 

.0006 

NaCl 

. 0097 

Ca 

.0279 

Na2S04  

.0120 

Mg 

. 0085 

CaH2C206 

.1129 

Na 

.0075 

MgTT2CnOc . . 

.0517 

Cl 

.0061 

S04 

.0081 

C03 

.1262 

NH3,  free 

trace 

NH3,  albuminoid 

none 

H,  bicarbonates 

.0020 

.2518 

.2518 

E,  two  artesian  well  waters  from  St.  Augustine,  Florida,  (a)  six- 
incli  well. 


Found. 

Per  cent, 
of  total. 

• 

Combina- 

tion. 

Suspended  matter. 

.0037 

.24 

Suspended  matter. 

.0037 

Si02 

.0224 

1.43 

Si02 

.0224 

A 1 2O3  

.0005 

.03 

A1203 

.0005 

Ca 

.1276 

8.16 

NaCl 

.6979 

Mg 

.0726 

4.  64 

KC1 

.0281 

Sr 

.0081 

.52 

MgCl2 

.1470 

Na 

.2743 

17.  54 

SrSOt 

.0170 

K 

.0147 

.94 

CaSO, 

.4338 

Cl 

.5469 

34. 97 

MgS04 

.0127 

S04 

.3253 

20.81 

MgHoC206  

.2007 

C03 

.1650 

10.  55 

OaTTjfJjOj - 

none. 

H,  bicarbonates... 

.0027 

.17 

1. 5638 

100. 00 

1. 5638 

60  WASHINGTON  LABORATORY.  [bull.  64. 

(b)  twelve-inch  well. 


Found. 

Per  cent, 
of  total. 

Combina- 

tion. 

Suspended  matter. 

.0016 

.05 

Suspended  matter . 

.-0016 

Si02 

.0280 

.88 

SiO« 

. 0280 

AljOj 

.0012 

' .04 

A1203 

.0012 

Ca 

.1755 

5.  50 

UaCl 

1. 9577 

Mg 

.1160 

3. 64 

KC1  

.0475 

Sr 

. 0089 

.28 

MeClo 

. 3534 

Na 

.7695 

24.12 

-1JAtevyx2  

SrS04 ... 

.0186 

K 

.0248 

.77 

CaS04 

. 4709 

Cl 

1. 4750 

46. 22 

M<rS04 

none. 

S04 

.3421 

10.  73 

Mp'TToCi.O* 

.1621 

C03 

.2442 

7.  64 

"Ah-LXzviv/6 

CaH2C2Oc 

.1499 

H,  bicarbonate  s . . . 

.0041 

.13 

3. 1909 

100. 00 

- 

3. 1909 

F,  from  well  four  miles  northwest  of  Clinton,  Hinds  County,  Missis- 
sippi. No  carbonates  present. 


Found. 

Percent, 
of  total. 

Combina- 

tion. 

• 

Suspended  matter. 

.0028 

.18 

Suspended  matter. 

.0028 

Sif)2 

.0750 

4.  82 

Si02 

.0750- 

Al2f)3 

.0077 

.49 

A1203  

.0077 

Fe^Oj 

trace. 

A1,(S04)* 

.0504 

A1  in  sulphate 

.0081 

.52 

MnSC>4 

.0028 

Mn 

. 0010 

.06  | 

CaS04  

.6732 

Ca 

.1980 

12.  72 

MgS04 

.3695 

Mer 

.0739 

4.  78 

^Ta.iSOj 

.2519 

"•o  - --  --  --  - 

Na 

. 1234 

7.  92 

NaCl 

. 1063 

K 

.0088 

.56 

KC1 

.0167 

S04 

.9852 

63.30 

Cl 

.0724 

4. 65 

1.  5563 

100.00 

1. 5563 

O 


Title  for  subject  entry.  Author  title.  Series  title. 


LIBRARY  CATALOGUE  SLIPS. 


United  States.  Department  of  the  interior.  ( U.  S.  geological  survey.) 
Department  of  the  interior  | — | Bulletin  | of  the  | United 
States  | geological  survey  | no.  65  | [Seal  of  the  department]  | 
Washington  | government  printing  office  | 1891 

Second  title:  United  States  geological  survey  | J.  W.  Powell, 
director  | — | Stratigraphy  | of  the  | bituminous  coal  field  | of  | 
Pennsylvania,  Ohio,  and  West  Virginia  | by  | Israel  C.  White  j . 
[Vignette]  | 

Washington  | government  printing  office  | 1891 

8°.  212  pp.  11  pL 


White  (Israel  C.). 

United  States  geological  survey  | J.  W.  Powell,  director  | — | 
Stratigraphy  | of  the  | bituminous  coal  field  | of  | Pennsylvania, 
Ohio,  and  West  Virginia  | by  | Israel  C.  White  | [Vignette] 
Washington  | government  printing  office  | 1891 

8°.  212  pp.  11  pi. 

[United  States.  Department  oj  the  interior.  ( U. . S.  geological  survey.) 
Bulletin  65.] 


United  States  geological  survey  | J.  W.  Powell,  director  | — | 
Stratigraphy  | of  the  | bituminous  coal  field  | of  | Pennsylvania, 
Ohio,  and  West  Virginia  | by  | Israel  C.  White  | [Vignette] 
Washington  | government  printing  office  | 1891 

8°.  212  pp.  11  pi. 

[United  States.  Department  qf  the  interior.  (U.  S.  geological  survey.) 
Bulletin  65.] 


ADYKETISEMENT 


[Bulletin  No.  65.] 


The  publications  of  the  United  States  Geological  Survey  are  issued  in  accordance  with  the  statute 
approved  March  3,  1879,  which  declares  that — 

“ The  publications  of  the  Geological  Survey  shall  consist  of  the  annual  report  of  operations,  geological 
and  economio  maps  illustrating  the  resources  and  classification  of  the  lands  and  reports  upon  general 
and  economic  geology  and  paleontology.  The  annual  report  of  operations  of  the  Geological  Survey 
shall  accompany  the  annual  report  of  the  Secretary  of  the  Interior.  All  special  memoirs  and  reports 
of  said  Survey  shall  be  issued  in  uniform  quarto  series  if  deemed  necessary  by  the  Director,  but  other- 
wise in  ordinary  octavos.  Three  thousand  copies  of  each  shall  be  published  for  scientific  exchanges 
and  for  sale  at  the  price  of  publication ; and  all  literary  and  cartographic  materials  received  in  exchange 
shall  be  the  property  of  the  United  States  and  form  a part  of  the  library  of  the  organization  • and  the 
money  resulting  from  the  sale  of  such  publications  shall  be  covered  into  the  Treasury  of  the  United 
States.” 

On  July  7, 1882,  the  following  joint  resolution,  referring  to  all  Government  publications,  was  passed 
by  Congress: 

“ That  whenever  any  document  or  report  shall  be  ordered  printed  by  Congress,  there  shall  be  printed, 
in  addition  to  the  number  in  each  case  stated,  the  ‘usual  number’  (1,900)  of  copies  for  binding  and 
distribution  among  those  entitled  to  receive  them.” 

Except  in  those  cases  in  which  an  extra  number  of  any  publication  has  been  supplied  to  the  Survey 
by  special  resolution  of  Congress  or  has  been  ordered  by  the  Secretary  of  the  Interior,  this  office  has 
no  copies  for  gratuitous  distribution. 

ANNUAL  REPORTS. 

L First  Annual  Report  of  the  United  States  Geological  Survey,  by  Clarence  King.  1880.  8°.  79  pp. 
1 map. — A preliminary  report  describing  plan  of  organization  and  publications. 

II.  Second  Annual  Report  of  the  United  States  Geological  Survey,  1880-81,  by  J.  W.  Powell.  1882. 
8°.  lv,  588  pp.  62  pi.  1 map. 

III.  Third  Annual  Report  of  the  United  States  Geological  Survey,  1881-’82,  by  J.  W.  Powell.  1883. 
8°.  xviii,  564  pp.  67  pi.  and  maps. 

TV.  Fourth  Annual  report  of  the  United  States  Geological  Survey,  1882-83,  by  J.  W.  Powell.  1884. 
8°.  xxxii,  473  pp.  85  pL  and  maps. 

Y.  Fifth  Annual  Report  of  the  United  States  Geological  Survey,  l883-’84,  by  J.  W.  Powell.  1885* 
8°.  xxxvi,  469  pp.  58  pi.  and  maps. 

YI.  Sixth  Annual  Report  of  the  United  States  Geological  Survey,  1884-’85,  by  J.  W.  Powell.  1885. 
8°.  xxix,  570  pp.  65  pi.  and  maps. 

VXL  Seventh  Annual  Report  of  the  United  States  Geological  Survey,  1885-’86,  by  J.  W.  Powell.  1888. 
8°.  xx,  656  pp.  71  pi.  and  maps. 

Tin.  Eighth  Annual  Report  of  the  United  States  Geological  Survey,  1886-’87,  by  J.  W.  Powell.  1889. 
8°  2v.  xix,  474,  xii  pp.  53  pi.  and  maps ; 1 p.  1.  475-1063  pp.  54-76  pi.  and  maps. 

IX.  Ninth  Annual  Report  of  the  United  States  Geological  Survey,  1887- ’88,  by  J.  W.  Powell.  1889. 
8°.  xiii,  717  pp.  88  pi.  and  maps. 

X.  Tenth  Annual  Report  of  the  United  States  Geological  Survey,  1888-’89,  by  J.  W.  Powell.  1890. 
8°.  2 v.  xv,  774  pp.  98  pi.  and  maps ; viii,  123  pp. 

The  Eleventh  Annual  Report  is  in  press. 

MONOGRAPHS. 

l.  Lake  Bonneville,  by  Grove  Karl  Gilbert.  1890.  4°.  xx,  438  pp.  51  pi.  1 map.  Price  $1.50. 

II.  Tertiary  History  of  the  Grand  Cafion  District,  with  atlas,  by  Clarence  E.  Dutton,  Capt.  U.  S.  A. 

]882.  4°.  xiv,  264  pp.  42  pi.  and  atlas  of  24  sheets  folio.  Price  $10.00. 

m.  Geology  of  the  Comstock  Lode  and  the  Washoe  District,  with  atlas  by  George  F.  Becker.  1882. 
4°.  xv,  422  pp.  7 pi.  and  atlas  of  21  sheets  folio.  Price  $11.00. 

IY.  Comstock  Mining  and  Miners,  by  Eliot  Lord.  1883.  4°.  xiv,  451  pp.  3 pi.  Price  $1.50. 

I 


II 


ADVERTISEMENT. 


V.  The  Copper-Bearing  Rocks  of  Lake  Superior,  by  Roland  Duer  Irving.  1883.  4®.  xvi,  464  pp. 
15  1.  29  pi.  and  maps.  Price  $1.85. 

VI.  Contributions  to  the  Knowledge  of  the  Older  Mesozoic  Flora  of  Virginia,  by  William  Morris 
Fontaine.  1883.  4°.  xi,  144  pp.  54 1.  54  pi.  Price  $1.05. 

VIL  Silver-Lead  Deposits  of  Eureka,  Nevada,  by  Joseph  Story  Curtis.  1884.  4°.  xiii,  200  pp.  16 
pi.  Price  $1.20 

Vin.  Paleontology  of  the  Eureka  District,  by  Charles  Doolittle  Walcott.  1884.  4°.  xiii,  298  pp. 
241.  24  pi.  Price  $1.10. 

IX.  Brachiopoda  and  Lamellibranchiata  of  the  Raritan  Clays  and  Greensand  Marls  of  New  Jersey, 
by  Robert  P.  Whitfield.  1885.  4°.  xx,  338  pp.  35  pi.  1 map.  Price  $1.15. 

X.  Dinocerata.  A Monograph  of  an  Extinct  Order  of  Gigantic  Mammals,  by  Othniel  Charles  Marsh. 
1886.  4°.  xviii,  243  pp.  56 1.  56  pi.  Price  $2.70. 

XI.  Geological  History  of  Lake  Lahontan,  a Quaternary  Lake  of  Northwestern  Nevada,  by  Israel 
Cook  Russell.  1885.  4°.  xiv,  288  pp.  46  pi.  and  maps.  Price  $1.75. 

XII.  Geology  and  Mining  Industry  of  Leadville,  Colorado,  with  atlas,  by  Samuel  Franklin  Emmons. 
1886.  4°.  xxix,  770  pp.  45  pi.  and  atlas  of  35  sheets  folio.  Price  $8.40. 

XIII.  Geology  of  the  Quicksilver  Deposits  of  the  Pacific  Slope,  with  atlas,  by  George  F.  Becker. 
1888.  4°.  xix,  486  pp.  7 pi.  and  atlas  of  14  sheets  folio.  Price  $2.00. 

XIV.  Fossil  Fishes  and  Fossil  Plants  of  the  Triassio  Rocks  of  New  Jersey  and  the  Connecticut  Val- 
ley, by  John  S.  Newberry.  1888.  4°.  xiv,  152  pp.  26  pi.  Price  $1.00. 

XV.  The  Potomac  or  Younger  Mesozoic  Flora,  by  William  Morris  Fontaine.  1889.  4°.  xiv,  377 
pp.  180  pi.  Text  and  plates  bound  separately.  Price  $2.50. 

XVI.  The  Paleozoic  Fishes  of  North  America,  by  John  Strong  Newberry.  1889.  4°.  340  pp.  53  pi. 
Price  $1.00. 

In  preparation : 

XVII.  The  Flora  of  the  Dakota  Group,  a posthumous  work,  by  Leo  Lesquereux.  Edited  by  F.  H. 
Knowlton. 

— Gasteropoda  of  the  New  Jersey  Cretaceous  and  Eocene  Marls,  by  R.  P.  Whitfield. 

— The  Penokee  Iron-Bearing  Series  of  Northern  Wisconsin  and  Michigan,  by  Roland  D.  Irving  and 
C.  R.  Van  Hise. 

— Mollusca  and  Crustacea  of  the  Mi&cene  Formations  of  New  Jersey,  by  R.  P.  Whitfield. 

— Geology  of  the  Eureka  Mining  District,  Nevada,  with  atlas,  by  Arnold  Hague. 

— Sauropoda,  by  O.  C.  Marsh. 

— Stegosauria,  by  O.  C.  Marsh. 

— Brontotheridae,  by  O.  C. Marsh. 

— Report  on  the  Denver  Coal  Basin,  by  S.  F.  Emmons. 

— Report  on  Silver  Cliff  and  Ten-Mile  Mining  Districts,  Colorado,  by  S.  F.  Emmons. 

— Flora  of  the  Dakota  Group,  by  J.  S.  Newberry. 

— The  Glacial  Lake  Agassiz,  by  Warren  Upham. 

BULLETINS. 

1.  On  Hypersthene- Andesite  and  on  Triclinic  Pyroxene  in  Augitio  Rocks,  by  Whitman  Cross,  with  a 
Geological  Sketch  of  Buffalo  Peaks,  Colorado,  by  S.  F.  Emmons.  1883.  8°.  42  pp.  2 pi.  Price  10  cents. 

2.  Gold  and  Silver  Conversion  Tables,  giving  the  coining  values  of  troy  ouncesof  fine  metal,  etc.,  com- 
puted by  Albert  Williams,  jr.  1883.  8°.  8 pp.  Price  5 cents. 

3.  On  the  Fossil  Faunas  of  the  Upper  Devonian,  along  the  meridian  of  76°  30',  from  Tompkins  County, 
New  York,  to  Bradford  County,  Pennsylvania,  by  Henry  S.  Williams.  1884.  8°.  36  pp.  Price  5 cents. 

4.  On  Mesozoic  Fossils,  by  Charles  A.  White.  1884.  8°.  36  pp.  9 pi.  Price  5 cents. 

5.  A Dictionary  of  Altitudes  in  the  United  States,  compiled  by  Henry  Gannett.  1884.  8°.  325  pp. 
Price  20  cents. 

6.  Elevations  in  the  Dominion  of  Canada,  by  J.  W.  Spencer.  1884.  8°.  43  pp.  Price  5 cents. 

7.  Mapoteca  Geologica  Americana.  A Catalogue  of  Geological  Maps  of  America  (North  and  South), 
1752-1881,  in  geographic  and  chronologic  order,  by  Jules  Marcou  and  John  Belknap  Marcou.  1884. 
8°.  184  pp.  Prioe  10  cents. 

8.  On  Secondary  Enlargements  of  Mineral  Fragments  in  Certain  Rocks,  by  R.  D.  Irving  and  C.  R. 
Van  Hise.  1884.  8°.  56  pp.  6 pi.  Price  10  cents. 

9.  A report  of  work  done  in  the  Washington  Laboratory  during  the  fiscal  year  1883-’84.  F.  W.  Clarke, 
chief  chemist.  T.  M.  Chatard,  assistant  chemist.  1884.  8°.  40  pp.  Price  5 cents. 

10.  On  the  Cambrian  Faunas  of  North  America.  Preliminary  studies,  by  Charles  Doolittle  Walcott. 
1884.  8°.  74  pp.  10  pi.  Prioe  5 cents. 

11.  On  the  Quaternary  and  Recent  Mollusca  of  the  Great  Basin  ; with  Descriptions  of  New  Forms,  by 
R.  Ellsworth  Call.  Introduced  by  a sketch  of  the  Quaternary  Lakes  of  the  Great  Basin,  by  G.  K. 
Gilbert.  1884.  8°.  66  pp.  6 pi.  Price  5 cents. 

12.  A Crystallographio  Study  of  the  Thinolite  of  Lake  Lahontan,  by  Edward  S.  Dana.  1884.  8°. 
34  pp.  3 pi.  Price  5 cents. 


ADVERTISEMENT. 


Ill 


13.  Boundaries  of  the  United  States  and  of  the  several  States  and  Territories,  with  a Historical 
Sketch  of  the  Territorial  Changes,  by  Henry  Gannett.  1885,  8°.  135  pp.  Price  10  cents. 

14.  The  Electrical  and  Magnetic  Properties  of  the  Iron-Carhnrets,  by  Carl  Barns  and  Vincent 
Strouhal.  1885.  8°.  238  pp.  Price  15  cents. 

15.  On  the  Mesozoic  and  Cenozoic  Paleontology  of  California,  by  Charles  A.  White.  1885.  8°. 
33  pp.  Price  5 cents. 

16.  On  the  Higher  Devonian  Faunas  of  Ontario  County,  Hew  York,  by  John  M.  Clarke.  1885.  8°. 
86  pp.  3 pi.  Price  5 cents. 

17.  On  the  Development  of  Crystallization  in  the  Igneous  Bocks  of  Washoe,  Nevada,  with  Notes  on 
the  Geology  of  the  District,  by  Arnold  Hague  and  Joseph  P.  Iddings.  1885.  8°.  44  pp.  Price  5 
cents. 

18.  On  Marine  Eocene,  Eresh-water  Miocene,  and  other  Fossil  Mollusca  of  Western  North  America, 
by  Charles  A.  White.  1885.  8°.  26  pp.  3 pi.  Price  5 cents. 

19.  Notes  on  the  Stratigraphy  of  California,  by  George  F.  Becker.  1885.  8°.  28  pp.  Price  5 cents. 

20.  Contributions  to  the  Mineralogy  of  the  Bocky  Mountains,  by  Whitman  Cross  and  W.  F.  Hille- 
brand.  1885.  8°.  114  pp.  1 pi.  Price  10  cents. 

21.  The  Lignites  of  the  Great  Sioux  Beservation.  A Beport  on  the  Begion  between  the  Grand  and 
Moreau  Bivers,  Dakota,  by  Bailey  Willis.  1885.  8°.  16  pp.  5 pi.  Price  5 cents. 

22.  On  New  Cretaceous  Fossils  from  California,  by  Charles  A.  White.  1885.  8°.  25  pp.  5 pi. 
Price  5 cents. 

23.  Observations  on  the  Junction  between  the  Eastern  Sandstone  and  the  Keweenaw  Series  on  Ke- 
weenaw Point,  Lake  Superior,  by  B.  D.  Irving  and  T.  C.  Chamberlin.  1885.  8°.  124  pp.  17  pi. 
Price  15  cents. 

24.  List  of  Marine  Mollusca,  comprising  the  Quaternary  Fossils  and  recent  forms  from  American 
Localities  between  Cape  Hatteras  and  Cape  Boque,  including  the  Bermudas,  by  William  Healey  Dali. 
1885.  8°.  336  pp.  Price  25  cents. 

25.  The  Present  Technical  Condition  of  the  Steel  Industry  of  the  United  States,  by  Phineas  Barnes. 
1885.  8°.  85  pp.  Price  10  cents. 

26.  Copper  Smelting,  by  Henry  M.  Howe.  1885.  8°.  107  pp.  Price  10  cents. 

27.  Beport  of  work  done  in  the  Division  of  Chemistry  and  Physics,  mainly  during  the  fiscal  year 

1884- ’85.  1886.  8°.  80  pp.  Price  10  cents. 

28.  The  Gabbros  and  Associated  Hornblende  Bocks  occurring  in  the  Neighborhood  of  Baltimore, 
Maryland,  by  George  Huntington  Williams.  1886.  8°.  78  pp.  4 pi.  Price  10  cents. 

29.  On  the  Fresh-water  Invertebrates  of  the  North  American  Jurassic,  by  Charles  A.  White.  1886. 
8°.  41  pp.  4 pi.  Price  5 cents. 

30.  Second  Contribution  to  the  Studies  on  the  Cambrian  Faunas  of  North  America,  by  Charles  Doo- 
little Walcott.  1886.  8°.  369  pp.  33  pi.  Price  25  cents. 

31.  Systematic  Beview  of  our  Present  Knowledge  of  Fossil  Insects,  including  Myriapods  and  Arach- 
nids, by  Samuel  Hubbard  Scudder.  1886.  8°.  128  pp.  Price  15  cents . 

32.  Lists  and  Analyses  of  the  Mineral  Springs  of  the  United  States;  a Preliminary  Study,  by  Albert 
C.  Peale.  1886.  8°.  235  pp.  Price  20  cents. 

33.  Notes  on  the  Geology  of  Northern  California,  by  J.  S.  Diller.  1886.  8°.  23  pp.  Price  5 cents. 

34.  On  the  relation  of  the  Laramie  Molluscan  Fauna  to  that  of  the  succeeding  Fresh-water  Eocene 
and  other  groups,  by  Charles  A.  White.  1886.  8°.  54  pp.-  5 pi.  Price  10  cents. 

35.  Physical  Properties  of  the  Iron-Carburets,  by  Carl  Barus  and  Vincent  Strouhal.  1886.  8°.  62 
pp.  Price  10  cents. 

36.  Subsidence  of  Fine  Solid  Particles  in  Liquids,  by  Carl  Barus.  1886.  8°.  58  pp.  Price  10  cents. 

37.  Types  of  the  Laramie  Flora,  by  Lester  F.  Ward.  1887.  8°.  354  pp.  57  pi.  Price  25  cents. 

38.  Peridotite  of  Elliott  County,  Kentucky,  by  J.  S.  Diller.  1887.  8°.  31pp.  I pi.  Price  5 cents. 

39.  The  Upper  Beaches  and  Deltas  of  the  Glacial  Lake  Agassiz,  by  Warren  Upham.  1887.  8°.  84 
pp.  1 pi.  Price  10  cents. 

40.  Changes  in  Biver  Courses  in  Washington  Territory  due  to  Glaciation,  by  Bailey  Willis.  1887. 
8°.  10  pp.  4 pi.  Price  5 cents. 

41.  On  the  Fossil  Faunas  of  the  Upper  Devonian — the  Genesee  Section,  New  York,  by  Henry  S. 
Williams.  1887.  8°.  121  pp.  4 pi.  Price  15  cents. 

42.  Beport  of  work  done  in  the  Division  of  Chemistry  and  Physics,  mainly  during  the  fiscal  year 

1885- ’86.  F.  W.  Clarke,  chief  chemist.  1887.  8°.  152  pp.  1 pi.  Price  15  cents. 

43.  Tertiary  and  Cretaceous  Strata  of  the  Tuscaloosa,  Tombigbee,  and  Alabama  Bivers,  by  Eugene 
A.  Smith  and  Lawrence  C.  Johnson.  1887.  8°.  189  pp.  21  pi.  Price  15  cents. 

44.  Bibliography  of  North  American  Geology  for  1886,  by  Nelson  H.  Darton.  1887.  8°.  35  pp. 
Price  5 cents. 

45.  The  Present  Condition  of  Knowledge  of  tho  Geology  of  Texas,  by  Robert  T.  Hill.  1887.  8°.  94 
pp.  Price  10  cents. 

46.  Nature  and  Origin  of  Deposits  of  Phosphate  of  Lime,  by  B.  A.  F.  Penrose,  jr.,  with  an  IntroduO' 
tion  by  N.  S.  Shaler.  1888.  8°.  143  pp.  Price  15  cents. 


IV 


ADVERTISEMENT. 


47.  Analyses  of  Waters  of  the  Yellowstone  National  Park,  with  an  Account  of  the  Methods  of  Anal- 
ysis employed,  by  Frank  Austin  Gooch  and  James  Edward  Whitfield.  1888.  8°.  84  pp.  Price  10 
cents. 

48.  On  the  Form  and  Position  of  the  Sea  Level,  by  Eobert  Simpson  Woodward.  1888.  8°.  88  pp. 
Price  10  cents. 

49.  Latitudes  and  Longitudes  of  Certain  Points  in  Missouri,  Kansas,  and  New  Mexico,  by  Eobert 
Simpson  Woodward.  1889.  8°.  133  pp.  Price  15  cents. 

50.  Formulas  and  Tables  to  facilitate  the  Construction  and  Use  of  Maps,  by  Eobert  Simpson  Wood- 
ward. 1889.  8°.  124  pp.  Price  15  cents. 

51.  On  Invertebrate  Fossils  from  the  Pacific  Coast,  by  Charles  Abiathar  White.  1889.  8°.  102  pp. 

14  pL  Price  15  cents. 

52.  Subaerial  Decay  of  Eocks  and  Origin  of  the  Eed  Color  of  Certain  Formations,  by  Israel  Cook 
Eussell.  1889.  8°.  65  pp.  5 pi.  Price  10  cents. 

53.  The  Geology  of  Nantucket,  by  Nathaniel  Southgate  Shaler.  1889.  8°.  55  pp.  10  pi.  Price  10 
cents. 

54.  On  the  Thermo-Electric  Measurement  of  High  Temperatures,  by  Carl  Barus.  1889.  8°.  313  pp. 
incl.  1 pi.  11  pi.  Price  25  cents. 

55.  Eeport  of  work  done  in  the  Division  of  Chemistry  and  Physics,  mainly  during  the  fiscal  yeat 

1886- 87.  Frank  Wigglesworth  Clarke,  chief  chemist.  1889.  8°.  96  pp.  Price  10  cents. 

56.  Fossil  Wood  and  Lignite  of  the  Potomac  Formation,  by  Frank  Hall  Knowlton.  1889.  8°.  72  pp. 
7 pi.  Price  10  cents. 

57.  A Geological  Eeconnaissance  in  Southwestern  Kansas,  by  Eobert  Hay.  1890.  8°.  49  pp.  2 pi. 
Price  5 cents. 

58.  The  Glacial  Boundary  in  Western  Pennsylvania,  Ohio,  Kentucky,  Indiana,  and  Illinois,  by  George 
Frederick  Wright,  with  an  introduction  by  Thomas  Chrowder  Chamberlin.  1890.  8°.  112  pp.  inch 
1 pi.  8 pi.  Price  15  cents. 

59.  The  Gabbros  and  Associated  Eocks  in  Delaware,  by  Frederick  D.  Chester.  1890.  8°.  45  pp. 
1 pi.  Price  10  cents. 

60.  Eeport  of  work  done  in  the  Division  of  Chemistry  and  Physics,  mainly  during  the  fiscal  year 

1887- 88.  F.  W.  Clarke,  chief  chemist.  1890.  8°.  174  pp.  Price  15  cents. 

61.  Contributions  to  the  Mineralogy  of  the  Pacific  Coast,  by  William  Harlow  Melville  and  Waldemar 
Lindgren.  1890.  8°.  40  pp.  3 pi.  Price  5 cents. 

62.  The  Greenstone  Schist  Areas  of  the  Menominee  and  Marquette  Eegions  of  Michigan ; a contri- 
bution to  the  subject  of  dynamic  metamorphism  in  eruptive  rocks,  by  George  Huntington  Williams; 
with  an  introduction  by  Eoland  Duer  Irving.  1890.  8°.  241  pp.  16  pi.  Price  30  cents. 

63.  A Bibliography  of  Paleozoic  Crustacea  from  1698  to  1889,  including  a list  of  North  American 
species  and  a systematic  arrangement  of  genera,  by  Anthony  W.  Yogdes.  1890.  8°.  177  pp.  Price 

15  cents. 

64.  A report  of  work  done  in  the  Division  of  Chemistry  and  Physics,  mainly  during  the  fiscal  year 
: 888-’89.  F.  W.  Clarke,  chief  chemist.  1890.  8°.  60  pp.  Price  10  cents. 

65.  Stratigraphy  of  the  Bituminous  Coal  Field  of  Pennsylvania,  Ohio,  and  West  Virginia,  by  Israel 
O.  White.  1891.  8°.  212  pp.  11  pi.  Price  20  cents. 

66.  On  a Group  of  Volcanic  Eocks  from  the  Tewan  Mountains,  New  Mexico,  and  on  the  occurrence 
* if  Primary  Quartz  in  certain  Basalts,  by  Joseph  Paxson  Iddings.  1890.  8°.  34  pp.  Price  5 cents. 

67.  The  relations  of  the  Traps  of  the  Newark  System  in  the  New  Jersey  Eegion,  by  Nelson  Horatio 
Darton.  1890.  8°.  82  pp.  Price  10  cents. 

68.  Earthquakes  in  California  in  1869,  by  James  Edward  Keeler.  1890.  8°.  25  pp.  Price  5 cents. 

69.  A Classed  and  Annotated  Bibliography  of  Fossil  Insects,  by  Samuel  Hubbard  Scudder.  1890. 
IP.  101  pp.  Price  15  cents. 

70.  Eeport  on  Astronomical  Work  of  1889  and  1890,  by  Eobert  Simpson  Woodward.  1890.  8°.  79 
pp.  Price  10  cents. 

71.  Index  to  the  Known  Fossil  Insects  of  the  World,  including  Myriapods  and  Arachnids,  by  Samuel 
Hubbard  Scudder.  1891.  8°.  744  pp.  Price  50  cents. 

In  press: 

72.  Altitudes  between  Lake  Superior  and  the  Eocky  Mountains,  by  Warren  Upham.  1891.  8°. 
229  pp.  Price  20  cents. 

73.  The  Viscosity  of  Solids,  by  Carl  Barus.  1891.  8°.  xii,  139  pp.  6 pi.  Price  15  cents. 

74.  The  Minerals  of  North  Carolina,  by  Frederick  Augustus  Genth.  1891.  8°.  119  pp.  Price  15 
cents. 

75.  Eecord  of  North  America  Geology  for  1887  to  1889,  inclusive,  by  Nelson  Horatio  Darton. 

76.  A Dictionary  of  Altitudes  in  the  United  States  (second  edition),  compiled  by  Henry  Gannett. 

77.  The  Texan  Permian  and  its  Mesozoic  types  of  Fossils,  by  Charles  A.  White.  1891.  8°.  51  pp. 
< pi.  Price  10  cents. 

78.  A report  of  work  done  in  the  Division  of  Chemistry  and  Physics,  mainly  during  the  fiscal  year 
!889-’90.  F.  W.  Clarke,  chief  chemist.  1891.  8°.  119  pp.  Price  15  cents. 

79.  A Late  Volcanic  Eruption  in  Northern  California  and  its  peculiar  lava,  by  J.  S.  Diller. 


ADVERTISEMENT. 


V 


80.  Correlation  papers— Devonian  and  Carboniferous,  by  Derry  Shaler  Williams. 

81.  Correlation  papers— Cambrian,  by  Charles  Doolittle  Walcott. 

82.  Correlation  papers  - Cretaceous,  by  Charles  A.  White. 

In  preparation : 

— The  Compressibility  of  Liquids,  by  Carl  Barus. 

— The  Eruptive  and  Sedimentary  Rocks  on  Pigeon  Point,  Minnesota,  and  their  contact  phenomena, 
by  W.  S.  Bayley. 

— A Bibliography  of  Paleobotany,  by  David  White. 

STATISTICAL  PAPERS. 

Mineral  Resources  of  the  United  States,  1882,  by  Albert  Williams,  jr.  1883.  8°.  xvii,  813  pp.  Price 
60  cents. 

Mineral  Resources  of  the  United  States,  1883  and  1884,  by  Albert  Williams,  jr.  1885.  8°.  xiv,  1016 
pp.  Price  60  cents. 

Mineral  Resources  of  the  United  States,  1885.  Division  of  Mining  Statistics  and  Technology.  1886. 
8°.  vii,  576  pp.  Price  40  cents. 

Mineral  Resources  of  the  United  States,  1886,  by  David  T.  Day.  1887.  8°.  viii,  813  pp.  Price  50 
cents. 

Mineral  Resources  of  the  United  States,  1887,  by  David  T.  Day.  1888.  8°.  vii,  832  pp.  Price  50 
cents. 

Mineral  Resources  of  the  United  States,  1888,  by  David  T.  Day.  1890.  8°.  vii,  652  pp.  Price  50 
cents. 

In  preparation : 

Mineral  Resources  of  the  United  States,  1889  and  1890. 

The  money  received  from  the  sale  of  these  publications  is  deposited  in  the  Treasury,  and  the  Secre- 
tary of  the  Treasury  declines  to  receive  bank  checks,  drafts,  or  postage  stamps;  all  remittances,  there- 
fore, must  be  by  postal  note  or  money  order,  made  payable  to  the  Librarian  of  the  U.  S.  Geological 
Survey,  or  in  currency,  for  the  exact  amount.  Correspondence  relating  to  the  publications  of  the 
Survey  should  be  addressed 

To  the  Director  of  the 

United  States  Geological  Survey, 

Washington,  D.  C. 

Washington,  D.  C.,  December,  1890 


DEPARTMENT  OF  THE  INTERIOR 


BULLETIN 

OF  THE 

UNITED  STATES 


GEOLOGICAL  SURVEY 


INo. 


6 5 


WASHINGTON 

GOVERNMENT  PRINTING  OFFICE 
1891 


UNITED  STATES  GEOLOGICAL  SURVEY 

J.  W.  POWELL,  DIRECTOR 


STRATIGRAPHY 


OF  THE 

/ 

BITUMINOUS  COAL  FIELD 


PENNSYLVANIA,  OHIO  AND  WEST  VIRGINIA 


BY 


ISRAEL  C.  WHITE 


WASHINGTON 

GOVERNMENT  PRINTING  OFFICE 
1891 


' 

. ...  ' ■ 


V 


- 


■ 

i; . ■■■  ■' ' 7 


. 


/ 


CONTENTS 


■ 


Page. 

Letter  of  transmittal 15 

Chap.  I. — Area,  structure,  and  classification  of  the  bituminous  coal  rocks 17 

Chap.  II. — The  Permo-Carboniferous  or  Dunkard  Creek  Measures 20 

Thickness,  character,  and  extent  20 

Section  on  Dunkard  Creek,  Greene  Co.,  Pa 22 

Section  on  Colvin’s  Run,  Greene  Co.,  Pa 23 

Section  in  Aleppo  Township,  Greene  Co.,  Pa 24 

Section  at  Board  Tree  Tunnel,  Marshall  Co.,  W.  Ya 25 

Section  at  Bellton,  Marshall  Co.,  W.  Ya 26 

Section  at  New  Martinsville,  Wetzel  Co.,  W.  Ya 27 

Section  at  Baresville,  Monroe  Co.,  Ohio 28 

Section  in  Liberty  Township,  Washington  Co.,  Ohio 29 

Section  at  Washington,  Washington  Co.,  Pa 29 

Section  near  Taylorstown,  Washington  Co.,  Pa 30 

Characteristic  horizons 30 

The  Windy  Gap  Limestone 30 

The  Windy  Gap  Coal 31 

The  Gilmore  Sandstone 31‘ 

The  Nineveh  Sandstone 32 

The  Bellton  Coal  Group 32 

The  Nineveh  Coal 32 

The  Nineveh  Limestone 32 

The  Hostetter  Coal 33 

The  Fish  Creek  Sandstone 33 

The  Dunkard  Coal 33 

The  Jollytown  Limestone 34 

The  Jollytown  Coal 34 

The  Upper  Washington  Limestone t 35 

The  Middle  Washington  Limestone 35 

The  Washington  “A”  Coal 35 

The  Marietta  Sandstones 35 

The  Blacksville  Limestone 36 

The  Lower  Washington  Limestone 36 

The  Washington  Coal 37 

Section  at  Farmington,  Marion  Co.,  W.  Va 37 

Section  on  Willey  Fork,  Wetzel  Co.,  W.  Va 38 

Section  near  Brown’s  Mill,  Monongalia  Co.,  W.  Va 38 

The  Washington  Sandstone 1 38 

The  Little  Washington  Coal 39 

The  Waynesburg  “ B”  Coal 39 

The  Colvin’s  Run  Limestone 39 

The  Waynesburg  “A”  Coal 39 

The  Mount  Morris  Limestone 39 

The  Waynesburg  Sandstone 40 

The  Cassville  Plant  Shale 41 

Age  of  the  Dunkard  Creek  Beds 41 


5 


6 


CONTENTS, 


Page. 

Chap.  III.  The  Upper  Coal  Measures,  or  Monongaliela  River  Series 43 

Thickness,  character,  and, extent 43 

Section  in  Fayette  and  Westmoreland  Cos.,  Pa 44 

Section  at  Brownsville,  Fayette  Co.,  Pa 44 

Section  at  West  Brownsville,  Washington  Co.,  Pa 45 

Section  at  Rice’s  Landing,  Greene  Co.,  Pa 45 

Section  on  Robinson’s  Run,  Monongalia  Co.,  W.  Va 46 

Section  on  Scott’s  Run,  Monongalia  Co.,  W.  Va ! 47 

Section  on  Buffalo  Creek,  Marion  Co.,  W.  Va 48 

Section  at  Clarksburg,  Harrison  Co.,  W.  Va 48 

Section  on  Chapline  Hill,  Wheeling,  W.  Va 49 

Section  near  Bellaire,  Belmont  Co.,  Ohio 50 

Section  at  Moundsville,  Marshall  Co  , W.  Ya 51 

Section  on  Pipe  Creek,  Belmont  Co.,  Ohio 51 

Section  in  Washington  Co.,  Ohio 52 

Section  at  Burning  Springs,  Wirt  Co.,  W.  Ya 52 

Section  on  Leading  Creek,  Gilmer  Co.,  W.  Ya 53 

Section  at  Antiquity,  Meigs  Co.,  Ohio 53 

Section  at  Hartford  City,  Mason  Co.,  W.  Ya 53 

Section  at  Arbuckle,  Mason  Co.,  W.  Va 54 

Section  at  mouth  of  Big  Hurricane  Creek,  Putnam  Co.,  W.  Ya  . ...  55 

Section  opposite  V^infield,  Putnam  Co.,  W.  Ya 5 o 

Section  near  Raymond  City,  Putnam  Co.,  W.  Ya 56 

Section  in  vicinity  of  Westernport,  Allegany  Co.,  Md 56 

Characteristic  horizons 57 

The  Waynesburg  Coal 57 

Iron  Ore 57 

The  Browntown  Sandstone 58 

The  Little  Waynesburg  Coal 58 

The  Waynesburg  Limestone 58 

The  Uniontown  Sandstone 58 

The  Uniontown  Coal 59 

The  Uniontown  Limestone 59 

The  “ Great”  Limestone 59 

The  Sewickley  Sandstone 60 

The  Sewickley  Coal 60 

The  Sewickley  Limestone 61 

The  Redstone  Coal 62 

The  Redstone  Limestone 62 

The  Pittsburgh  Saudstone 63 

The  Pittsburgh  Coal 63 

Section  at  Newburgh,  Preston  Co.,  W.  Va 65 

Section  in  Copeman’s  Knob,  Preston  Co.,  W.  Va 65 

Section  at  Fairfax  Knob,  Tucker  Co.,  W.  Ya 65 

Section  at  Huntington,  Cabell  Co.,  W.  Ya 66 

Section  at  Pomeroy,  Ohio 66 

Section  on  Shade  Creek,  Meigs  and  Athens  Cos.,  Ohio 66 

Section  on  Federal  Creek,  Athens  and  Morgan  Cos.,  Ohio 67 

Section  at  Berry’s  mine,  in  Homer  Township,  Morgan  Co.,  Ohio  ..  67 

Section  in  Washington  Township,  Belmont  Co.,  Ohio • 67 

Section  at  Heatherington’s  mine,  at  Bellaire,  Belmont  Co.,  Ohio ..  68 

Section  in  Warren  Township,  Jefferson  Co.,  Ohio 68 

Section  in  German  Township,  Harrison  Co.,  Ohio 68 

Section  at  Columbia  mine,  Westmoreland  Co.,  Pa 68 

Fossils  of  the  Upper  Coal  Measures 69 


CONTENTS. 


7 


Page. 

Chap.  IV.  The  Barren  Measures,  or  Elk  River  Series 70 

Thickness,  character,  and  extent 70 

Section  in  Pittsburgh  region 72 

Section  at  Sewickley,  Pa 73 

Section  on  Dunbar  Creek,  Fayette  Co.,  Pa 74 

Section  at  Ligonier,  Westmoreland  Co.,  Pa 75 

Section  in  vicinity  of  Berlin,  Somerset  Co.,  Pa 76 

Section  in  Broad  Top  Basin,  Bedford  Co.,  Pa 76 

Section  opposite  Steubenville,  Ohio 77 

Section  under  Washington,  Pa 77 

Section  near  Cannonsburg,  Washington  Co.,  Pa 78 

Section  at  Morgantown,  W.  Ya 79 

Section  near  Little  Falls,  Monongalia  Co.,  W.  Va 80 

Section  at  Newburg,  Preston  Co.,  W.  Ya 81 

Section  at  Fairfax  Knob,  Tucker  Co.,  W.  Va 82 

Section  in  Guernsey  Co.,  Ohio 83 

Section  at  Burning  Springs,  Wirt  Co.,  W.  Ya 83 

Section  in  vicinity  of  Huntington,  W.  Va 84 

Section  near  Charleston,  W.  Ya 85 

Characteristic  horizons 86 

The  Pittsburgh  Coal  Ores 86 

The  Little  Pittsburgh  Coal 86 

The  Pittsburgh  Limestones 87 

The  Connellsville  Sandstone 87 

The  Little  Clarksburg  Coal 88 

The  Clarksburg  Limestone 88 

The  Morgantown  Sandstone 88 

The  Elk  Lick  Coal 89 

Thb  Elk  Lick  Limestone 90 

The  Crinoidal,  Green  Fossiliferous,  or  Ames  Limestone 90 

The  Crinoidal  Coal 91 

The  Red  Shale  Beds 92 

The  Bakersto  wn  Coal 92 

The  Cambridge  Li mestoues 93 

The  Masontown  Coal 94 

The  Irondale  Limestone  and  Ore 95 

The  Mahoning  Sandstone 95 

The  Mahoning  Coal 96 

The  Mahoning  Limestone . 96 

The  Upper  and  Middle  Cannelton  Coals 97 

The  Kanawha  Black  Flint 98 

Chap.  V.  The  Lower  Coal  Measures,  or  Alleghany  River  Series 99 

Thickness,  character,  and  extent 99 

Section  at  Blossburg,  Tioga  Co.,  Pa 102 

Section  at  Fall  Brook,  Tioga  Co.,  Pa 103 

Section  at  Karthaus,  Clearfield  Co.,  Pa 103 

Section  in  Horton  Towriship,  Elk  Co.,  Pa 104 

Section  at  Brockwayville,  Jefferson  Co.,  Pa.. 104 

Section  in  Clarion  Co.,  Pa 105 

Section  at  Miller’s  Eddy,  Clarion  Co.,  Pa 105 

Section  at  East  Brady,  Clarion  Co.,  Pa 106 

Section  near  New  Bethlehem,  Clarion  Co.,  Pa 106 

Section  in  Brady  Township,  Butler  Co.,  Pa 107 

Section  at  Ore  Hill  Furnace,  Armstrong  Co.,  Pa 107 

Section  at  Centerville,  Armstrong  Co.,  Pa.„ 108 


8 


CONTENTS, 


Page. 

Chap.  V.  The  Lower  Coal  Measures,  or  Alleghany  River  Series— Continued. 

Section  at  Putney  ville,  Armstrong  Co.,  Pa 108 

Section  in  vicinity  of  Kittanning,  Pa 100 

Section  5 miles  below  Kittanning,  Pa 109 

Section  at  Logansport,  Armstrong  Co.,  Pa 110 

Section  at  Freeport,  Armstrong  Co.,  Pa  Ill 

Section  near  mouth  of  Beaver  River 112 

Section  under  Sewickley,  Allegheny  Co.,  Pa 112 

Section  under  Washington,  Pa 113 

Section  near  Carpenter’s  Station,  Westmoreland  Co.,  Pa 113 

Section  under  Murraysvilie,  Westmorelaud  Co.,  Pa 114 

Section  on  Beaver  Run,  Westmoreland  Co.,  Pa 114 

Section  near  Richmond,  Indiana  Co.,  Pa 115 

Section  near  Lockport  and  Bolivar,  Indiana  Co.,  Pa 115 

Section  near  Laughlinton,  Westmoreland  Co.,  Pa 116 

Section  on  Cucumber  Run,  Stewart  Township,  Fayette  Co.,  Pa 116 

Section  under  Newburg,  Preston  Co.,  W.  Ya 117 

Section  near  Johnstown,  Cambria  Co.,  Pa 118 

Section  at  Conemaugh,  near  Johnstown,  Cambria  Co.,  Pa 119 

Section  in  Jackson  Township,  Cambria  Co.,  Pa 119 

Section  on  Ben’s  Creek,  Cambria  Co.,  Pa 120 

Section  at  Stoyestown,  Somerset  Co.,  Pa 121 

Section  at  Pinkerton  Point,  Somerset  Co.,  Pa 121 

Section  at  Cresson,  Cambria  Co.,  Pa 122 

Section  at  Bennington,  Blair  Co.,  Pa 122 

Section  at  Clearfield, "Clearfield  Co.,  Pa 123 

Section  near  Morrisdale,  Clearfield  Co.,  Pa 123 

Section  at  Sterling  mines,  near  Houtzdale,  Clearfield  Co.,  Pa 124 

Section  on  Shoup’s  Run,  Broad  Top  Basin,  Huntingdon  Co.,  Pa 125 

Section  in  East  Broad  Top  Basin,  Huntingdon  Co.,  Pa 125 

Section  in  Broad  Top  Basin,  Bedford  Co.,  Pa 126 

Section  at  Piedmont,  Mineral  Co.,  W.  Ya 126 

Section  at  Maple  Swamp  water  tank,  W.  Ya.  Central  Railroad 127 

Section  near  Thomas,  Tucker  Co.,  W.  Ya 127 

Section  near  Moatsville,  Barbour  Co.,  W.  Va 128 

Section  at  Yalley  Falls,  Taylor  Co.,  W.  Va 128 

Section  near  Nuzum’s  Mills,  Marion  Co.,  W.  Va 129 

Section  under  Clarksburg,  Harrison  Co.,  W.  Ya 129 

Section  under  Parkersburg,  W.  Va 130 

Section  under  Wheeling,  W.  Va 130 

Section  at  mouth  of  Little  Beaver,  on  the  Ohio-Penusylvauia  line 130 

Section  near  Sprucevale,  Columbiana  Co.,  Ohio 131 

Section  between  New  Lisbon  and  Leetonia,  Ohio 132 

Section  at  Zanesville,  Muskingum  Co.,  Ohio 132 

Section  in  vicinity  of  Shawnee  and  McCuneville,  Perry  Co.,  Ohio 133 

Section  in  Hocking  Yalley,  near  Buchtel,  Ohio 133 

Section  on  Meeker’s  Run,  near  Nelsonville,  Athens  Co.,  Ohio 134 

Section  in  Panther  Hill,  Mt.  Vernon  Furnace,  Scioto  Co.,  Ohio 134 

Section  at  Ironton,  Lawrence  Co.,  Ohio 135 

Section  in  southern  Ohio,  above  Ironton , 135 

Section  under  Charleston,  W.  Ya 136 

Section  at  mouth  of  Lick  Run,  2 miles  above  Charleston,  W.  Va 137 

Section  at  Dickinson  Salt  Works,  Kanawha  Co.,  W.  Va 138 

Section  near  Brownstown,  3 miles  south  from  Malden,  W.  Ya 139 

Section  at  mouth  of  Armstrong  Creek,  on  the  Big  Kanawha  River 140 


CONTENTS, 


9 


Page. 

Chap.  V.  The  Lower  Coal  Measures,  or  Alleghany  River  Series — Continued. 

Section  at  Guyandotte  Mountain,  Raleigh  Co.,  W.  Va 142 

Section  near  Oceana,  Wyoming  Co.,  W.  Va 143 

Section  at  mouth  of  Blaine  Creek,  Lawrence  Co.,  Ky 144 

Section  near  Old  Peach  Orchard,  Ky 145 

Section  at  Warfield,  Ky.,  and  on  Tug  Fork  of  Big  Sandy  River. ..  146 

Section  on  Tug  Fork  of  Big  Sandy  River,  Logan  Co.,  W.  Va 147 

Characteristic  horizons 147 

The  Upper  Freeport  Coal 147 

Section  at  McCoy  Shaft,  near  Gallitzin,  Cambria  Co.,  Pa 148 

Section  near  old  Portage  Railroad  tunnel,  at  Gallitzin,  Pa 149 

Section  at  Mt.  Equity  mine,  Bedford  Co.,  Pa 149 

Section  at  Posten’s  bank,  near  Masontown,  Preston  Co.,  W.  Va...  150 

Section  at  Hartley’s  bank,  near  Masontown,  W.  Va 150 

Section  at  Wilson’s  mine,  Roaring  Creek,  Randolph  Co.,W.  Va  ..  151 

Section  on  Stone  Coal  Run,  Upshur  Co.,  W.  Va 151 

Section  on  the  Buckhannon  River,  Upshur  Co.,  W.  Va 152 

Section  at  Lloyd  Wamsley’s  bauk,  Upshur  Co.,  W.  Va 152 

Section  at  Bryan’s  bank,  Upshur  Co.,  W.  Va 152 

Section  at  Current’s  farm,  Upshur  Co.,  W.  Va 152 

Section  near  Hacker’s  Valley  post-office,  Webster  Co.,  W.  Va 153 

Section  on  the  Little  Kahawha  River,  Webster  Co.,  W.  Va 153 

Section  on  the  Holly  River,  Webster  Co.,  W.  Va 153 

Section  at  Powell  Mountain,  Nicholas  Co.,  W.  Va 153 

Section  on  Stroud  Creek,  Nicholas  Co.,  W.  Va 154 

Sections  on  Mumble-the-Peg  Creek,  Nicholas  Co.,  W.  Va 154 

Sections  on  the  Guyandotte  River,  Cabell  Co.,  W.  Va 155 

Sections  on  Cove  Creek,  Wayne  Co.,  W.  Va 155 

Section  on  Twelve-pole  Creek,  Wayne  Co.,  W.  Va 156 

Section  on  Little  Laurel  Creek,  Wayne  Co.,  W.  Va 156 

Section  on  Saw-pit  branch  of  Cove  Creek,  Wayne  Co.,  W.  Va 157 

Section  in  Sugar  Camp  Hollow,  Wayne  Co.,  W Va 157 

Section  on  Trough  Creek,  Wayne  Co.,  W.  Va 157 

Section  at  Greene  Porter’s,  Twelve-pole  Creek,  Wayne  Co.,  W.  Va.  158 

Section  near  Kenova,  W.  Va 158 

Section  in  Ritchie  Co.,  W.  Va 159 

The  Upper  Freeport  Limestone 159 

The  Bolivar  Fireclay 159 

The  Upper  Freeport  Sandstone 160 

The  Middle  Freeport  Coal.. 160 

The  Lower  Freeport  Coal 160 

Section  near  Philippi,  Barbour  Co.,  W.  Va 161 

Section  of  bed  at  Coalburg,  Kanawha  Co.,  W.  Va 162 

Section  at  Winifrede,  Kanawha  Co.,  W.  Va 162 

Section  at  mouth  of  Blaine  Creek,  Lawrence  Co.,  Ky 162 

The  Lower  Freeport  Limestone 163 

The  Lower  Freeport  Sandstone 163 

The  Upper  Kittauning  Coal 164 

The  Johnstown  (Cement)  Limestone 165 

The  Middle  Kittanning  Coal 166 

Section  at  Newburg,  Preston  Co.,  W.  Va 167 

Section  in  Hocking  Valley,  Ohio 168 

Section  at  New  Straits ville,  Perry  Co.,  Ohio 168 

The  Lower  Kittanning  Coal 169 

Section  at  Newburg,  Preston  Co.,  W.  Va 170 


10  CONTENTS. 

Page. 


Chap.  V.  The  Lower  Coal  Measures,  or  Alleghany  River  Series — Continued. 

The  Kittanning  Fire-clay 171 

The  Kittanning  Sandstone 172 

The  Buhrstone  Iron  Ore 172 

The  Ferriferous  Limestone  173 

The  Clarion  Coal 175 

Section  near  Eagle,  Fayette  Co.,  W.  Va 176 

The  Eagle  Limestone 177 

The  Brookville  Coal 178 

Chap.  VI.  The  Pottsville  Conglomerate  Series 179 

Thickness,  character,  and  extents 179  . 

Section  in  Fox  Township,  Elk  Co.,  Pa 182 

Section  near  Clearfield,  Pa 182 

Section  at  Brookville,  Jefferson  Co.,  Pa 183 

Section  at  Patton  Station,  Red  Bank  Township,  Clarion  Co.,  Pa.  183 

Section  at  Kellersburg,  Armstrong  Co.,  Pa 184 

Section  under  Pittsburgh,  Pa 184 

Section  under  Murraysville,  Pa 184 

Section  under  Washington,  Pa 185 

Section  in  the  Broad  Top  Basin,  Huntingdon  Co.,  Pa 185 

Section  near  Wellersburg,  Somerset  Co.,  Pa 186 

Section  near  Piedmont,  Mineral  Co.,  W.  Va 186 

Section  on  Black  Fork  of  Cheat  River,  Tucker  Co.,  W.  Va 187 

Section  near  Rowlesburgh,  Preston  Co.,  W.  Va 188 

Section  near  mouthy  of  Sandy  Creek,  Preston  Co.,  W.  Va 188 

Section  on  Booth’s  Creek,  Taylor  Co.,  W.  Va 189 

Section  under  Clarksburg,  W.  Va  189 

Section  near  Farmington,  W.  Va 189 

Section  under  Wellsburg,  W.  Va 190 

Section  in  Mercer  Co.,  Pa 190 

Section  near  Quakertown,  Mahoning  Co.,  Ohio 191 

Section  in  Holmes  Co.,  Ohio 191 

Section  in  Washington  Co.,  Ohio 192 

Section  under  Parkersburg,  W.  Va 192 

Section  near  Burning  Springs,  Wirt  Co.,  W.  Va 192 

Section  at  Jackson  Furnace,  Jackson  Co.,  Ohio 193 

Section  at  Hanging  Rock,  Scioto  Co.,  Ohio 193 

Section  on  Big  Sandy  River,  at  mouth  of  Blaine  Creek 194 

Section  under  Charleston,  Kanawha  Co.,  W.  Va 195 

Section  at  Burning  Spring,  Kanawha  Co.,  W.  Va 196 

Section  near  Nuttallburg,  Fayette  Co.,  W.  Va  167 

Section  on  Crane  Creek,  Mercer  Co.,  W.  Va 198 

Characteristic  horizons 199 

The  Homewood  Sandstone 199 

The  Mercer  Group 200 

The  Connoquenessing  Sandstones 201 

The  New  River  Coal  Group 202 

Section  on  Crane  Creek,  near  Pocahontas,  Va 203 

Section  at  head  of  South  Elk  Horn  Creek,  McDowell  Co.,  W.  Val.  203 

Section  on  East  Branch  of  Simmon’s  Creek,  Mercer  Co.,  W.  Va 203 

Section  on  Walker  tract,  Flipping  Creek,  Mercer  Co.,  W.  Va 204 

Section  on  Pinnacle  Fork  of  Guyaudotte  River,  Mercer  Co.,  W.  Va  204 

The  Sharon  Conglomerate 204 

The  Lower  Carboniferous  Beds 205 


ILLUSTRATIONS. 


Page. 

Plate  I.  Map  showing  the  general  distribution  of  the  Carboniferous  in  Penn- 
sylvania, West  Virginia,  and  Ohio Frontispiece. 

II.  Sections  across  the  Appalachian  Coal  Fields.  Figs.  1 and  2 16 

III.  Sections  across  the  Appalachian  Coal  Fields,  from  Ravenna,  Ohio, 

to  the  Alleghany  mountains 18 

IV.  Permo-Carboniferous,  Cameron,  W.  Va 20 

V.  Upper  Coal  Measures,  capped  with  Permo-Carboniferous  beds,  Wheel- 
ing, W.  Va 44 

VI.  Upper  Coal  Measures  and  Permo-Carboniferous,  Powhatan,  Ohio...  50 

VII.  Upper  Coal  Measures  at  Point  Pleasant,  W.  Va 60 

VIII.  The  Pittsburgh  coal  outcrop  near  Connellsville,  Pa 64 

IX.  Lower  Coal  Measures,  Coalburg,  Kanawha  River,  W.  Va 100 

X.  The  Pottsville  conglomerate  topography  in  Blackwater  Canyon 180 

XI.  The  Pottsville  conglomerate  cliifs  and  d6bris,  New  River,  West  Vir- 
ginia   202 

Fig.  1.  Section  on  Dunkard  Creek,  Greene  Co.,  Pa 22 

2.  Section  on  Colvin’s  Run,  Greene  Co.,  Pa 23 

3.  Section  in  Aleppo  Township,  Greene  Co.,  Pa 24 

4.  Section  at  Board  Tree,  Marshall  Co.,  W.  Va 25 

5.  Section  at  Bellton,  Marshall  Co.,  W.  Va 26 

6.  Section  at  New  Martinsville,  Wetzel  Co.,  W.  Va 27 

7.  Section  at  Baresville,  Monroe  Co.,  Ohio 28 

8.  Section  in  Liberty  Township,  Washington  Co.,  Ohio 29 

9.  Section  at  Washington,  Washington  Co.,  Pa 29 

10.  Section  near  Taylorstown,  Washington  Co.,  Pa 30 

, 11.  Section  in  Fayette  and  Westmoreland  Cos.,  Pa 44 

12.  Section  at  Brownsville,  Fayette  Co.,  Pa 44 

33.  Section  at  West  Brownsville,  Washington  Co.,  Pa 45 

14.  Section  at  Rice’s  Landing,  Greene  Co.,  Pa 45 

15.  Section  on  Robinson’s  Run,  Monongalia  Co.,  W.  Va 46 

16.  Section  on  Scott’s  Run,  Monongalia  Co.,  W.  Va 47 

17.  Section  on  Buffalo  Creek,  Marion  Co.,  W.  Va 48 

18.  Section  at  Clarksburg,  Harrison  Co.,  W.  Va 49 

19.  Section  on  Chapline  Hill,  Wheeling,  W.  Va 49 

20.  Section  near  Bellaire,  Ohio 50 

21.  Section  at  Moundsville,  W.  Va 51 

22.  Section  on  Pipe  Creek,  Belmont  Co.,  Ohio 51 

23.  Section  in  Washington  Co.,  Ohio  52 

24.  Section  at  Burning  Springs,  Wirt  Co.,  W.  Va 52 

25.  Section  on  Leading  Creek,  Gilmer  Co.,  W.  Va  . ... 53 

26.  Section  at  Antique,  Meigs  Co.,  Ohio : 53 

27.  Section  at  Hartford  City,  Mason  Co.,  W.  Va 54 

28.  Section  at  Arbuckle,  Mason  Co.,  W.  Va 54 


11 


12 


LIST  OP  ILLUSTRATIONS. 


Fig.  29.  Section  at  month  of  Big  Hurricane  Creek,  Putnam  Co.,  W.  Va 

30.  Section  opposite  Winfield,  Putnam  Co.,  W.  Va 

31.  Section  n^ar  Raymond  City,  W.  Va P - 

32.  Section  in  vicinity  of  Westernport,  Md ... 

33.  Section  in  the  Pittsburgh  region '.... 

34.  Section  at  Sewickley,  Fa 

35.  Section  on  Dunbar  Creek,  Fayette  Co.,  Pa w 

36.  Section  at  Ligonier,  Westmoreland  Co.,  Pa 

37.  Section  in  vicinity  of  Berlin,  Somerset  Co.,  Pa 

38.  Section  at  Broad  Top,  Bedford  Co.,  Pa 

39.  Section  opposite  Steubenville,  Ohio 

40.  Section  at  Washington,  Pa  

41.  Section  near  Cannonsburg,  Washington  Co.,  Pa 

42.  Section  at  Morgantown,  W.  Va 

43.  Section  at  Little  Falls,  Monongalia  Co.,  W.  Va 

44.  Section  at  Newburg,  Preston  Co.,  W.  Va 

45.  Section  at  Fairfax  Knob,  Tucker  Co.,  W.  Va 

46.  Section  in  Guernsey  Co.,  Ohio 

47.  Section  at  Burning  Springs,  Wirt  Co.,  W.  Va 

48.  Section  near  Huntington,  W.  Va 

49.  Section  near  Charleston,  W.  Va 

50.  Section  at  Blossburg,  Tioga  Co.,  Pa  

51.  Section  at  Fall  Brook,  Tioga  Co.,  Pa  

52.  Section  at  Karthaus,  Clearfield  Co.,  Pa. 

53.  Section  in  Horton  Township,  Elk  Co.,  Pa 

54.  Section  at  Brock  way  ville,  Jefferson  Co.,  Pa 

55.  Section  in  Clarion  Co.,  Pa 

56.  Section  at  Miller’s  Eddy,  Clarion  Co.,  Pa ... 

57.  Section  at  East  Brady,  Clarion  Co.,  Pa 

58.  Section  near  New  Bethlehem,  Clarion  Co.,  Pa 

59.  Section  in  Brady  Township,  Butler  Co.,  Pa 

60.  Section  near  Ore  Hill  Furnace,  Armstrong  Co.,  Pa 

61.  Section  at  Centerville,  Armstrong  Co.,  Pa 

62.  Section  at  Putney ville,  Armstrong  Co.,  Pa 

63.  Section  near  Kittanning,  Pa 

64.  Section  5 miles  below  Kittanning,  Pa : 

65.  Section  at  Logansport,  Armstrong  Co.,  Pa 

66.  Section  at  Freeport,  Pa 

67.  Section  near  mouth  of  Beaver  River,  Pa 

68.  Section  at  Sewickley,  Allegheny  Co.,  Pa 

69.  Section  under  Washington,  Pa 

70.  Section  near  Carpenter’s  Station,  Westmoreland  Co.,  Pa 

71.  Section  under  Murraysville,  Westmoreland  Co.,  Pa 

72.  Section  on  Beaver  Run,  Westmoreland  Co.,  Pa 

73.  Section  near  Richmond,  Indiana  Co.,  Pa 

74.  Section  near  Lockport  and  Bolivar,  Indiana  Co.,  Pa 

75.  Section  on  Laurel  Run,  near  Laughlintown,  Westmoreland  Co.,  Pa  .. 

76.  Section  on  Cucumber  Run,  Stewart  Township,  Fayette  Co.,  Pa 

77.  Section  at  Newburg,  Preston  Co.,  W.  Va 

78.  Section  at  Johnstown,  Cambria  Co.,  Pa 

79.  Section  at  Conemaugu,  near  Johnstown,  Pa  . . ' 

80.  Section  in  Jackson  Township,  Cambria  Co.,  Pa.. 

81.  Section  on  Ben’s  Creek,  Cambria  Co.,  Pa 

82.  Section  near  Stoyestown,  Somerset  Co.,  Pa 

83.  Section  at  Pinkerton  Point,  Somerset  Co.,  Pa 


Page. 

55 

55 

56 
56 

72 

73 

74 

75 

76 

77 

77 

78 

78 

79 

80 
81 
82 
83 

83 

84 

85 
1(2 
103 

103 

104 

104 

105 

105 

106 
106 
107 

107 

108 
108 
109 

109 

110 
111 
112’ 
112 
113 

113 

114 

114 

115 

115 

116 
116 

117 

118 
119 

119 

120 
121 
121 


LIST  OF  ILLUSTRATIONS.  13 

Page. 

Fig.  84.  Section  at  Cresson,  Pa 122 

85.  Section  at  Bennington,  Blair  Co.,  Pa 122 

86.  Section  at  Clearfield,  Clearfield  Co.,  Pa  123 

87.  Section  near  Morriedale,  Clearfield  Co.,  Pa 123 

88.  Section  at  Sterling  mines,  near  Houtzdale,  Clearfield  Co.,  Pa 124 

89.  Section  on  Shoup’s  Run,  Broad  Top  Basin,  Huntingdon  Co.,  Pa 125 

90.  Section  East  Broad  Top  Basin,  Huntingdon  Co.,  Pa 125 

91.  Section  in  Broad  Top  Basin,  Bedford  Co.,  Pa 126 

92.  Section  at  Piedmont,  Mineral  Co.,  W.  Ya 126 

93.  Section  on  North  Potomac,  at  Maple  Swamp  Water  Tank,  West  Vir- 

ginia Central  Railroad 127 

94.  Section  near  Thomas,  Tucker  Co.,  W.  Va 127 

95.  Section  near  Moatsville,  Barbour  Co.,  W.  Ya 128 

96.  Section  at  Valley  Falls,  Taylor  Co.,  W.  Va.. 128 

97.  Section  near  Nuzum’s  Mills,  Marion  Co.,  W.  Va 129 

98.  Section  under  Clarksburg,  W.  Va 129 

99.  Section  under  Parkersburgh,  W.  Va 130 

100.  Section  under  Wheeling,  W.  Va 130 

101.  Section  at  mouth  of  Little  Beaver,  on  the  Ohio-Pennsylvania  line 130 

102.  Section  near  Sprucevale,  Columbiana  Co.,  Ohio 131 

103.  Section  between  New  Lisbon  and  Leetonia,  Ohio 132 

104.  Section  at  Zanesville,  Muskingum  Co.,  Ohio 132 

105.  Section  in  vicinity  of  Shawnee  and  McCuneville,  Perry  Co.,  Ohio...  133 

106.  Section  in  Hocking  Valley,  near  Buchtel,  Ohio 133 

107.  Section  on  Meeker’s  Run,  near  Nelsonville,  Athens  Co.,  Ohio 134 

108.  Section  in  Panther  Hill,  Mt.  Vernon  Furnace,  Scioto  Co.,  Ohio 134 

109.  Section  at  Ironton,  Ohio 135 

110.  Section  in  southern  Ohio,  above  Ironton ^ 135 

111.  Section  under  Charleston,  W.  Va 136 

112.  Section  at  mouth  of  Lick  Run,  2 miles  above  Charleston,  W.  Va 137 

113.  Section  at  Dickinson  salt  works,  Kanawha  Co.,  W.  Va 138 

114.  Section  near  Brownstown,  3 miles  south  from  Malden 139 

115.  Section  at  mouth  of  Armstrong  Creek,  on  the  Big  Kanawha  River...  140 

116.  Section  at  Guyandotte  Mountain,  Raleigh  Co.,  W.  Va 142 

117.  Section  near  Oceana,  Wyoming  Co.,  W.  Va 143 

118.  Section  at  mouth  of  Blaine  Creek,  20  miles  above  mouth  of  Big 

Sandy  River,  Lawrence  Co.,  Ky 144 

119.  Section  near  Peach  Orchard,  Lawrence  Co.,  Ky 145 

120.  Section  near  Warfield,  Ky.,  on  Tug  Fork  of  Big  Sandy  River 146 

121.  Section  on  Tug  Fork  of  Big  Sandy  River,  near  mouth  of  Knox  Creek, 

southern  edge  of  Logan  Co.,  W.  Va 147 

122.  Section  in  Fox  Township,  Elk  Co.,  Pa 182 

123.  Section  at  Clearfield,  Pa 183 

124.  Section  at  Brookville,  Jefferson  Co.,  Pa 183 

125.  Section  at  Patton  Station,  Red  Bank  Township,  Clarion  Co.,  Pa  ...  183 

126.  Section  at  Kellersburgh,  Armstrong  Co.,  Pa 184 

127.  Section  under  Pittsburgh,  Pa 184 

128.  Section  under  Murray sville,  Pa 185 

129.  Section  under  Washington,  Pa 185 

130.  Section  in  the  Broad  Top  Basin,  Huntingdon  Co.,  Pa 185 

131.  Section  on  Gladden’s  Run,  near  Wellersburg,  Somerset  Co.,  Pa 186 

132.  Section  near  Piedmont,  Mineral  Co.,  W.  Va 186 

133.  Section  on  Black  Fork  of  Cheat  River,  Tucker  Co.,  W.  Va 187 

134.  Section  along  the  Baltimore  and  Ohio  Railroad,  Cheat  River  grade, 

4 miles  west  from  Rowlesburgh,  Preston  Co.,  W.  Va 188 


‘ 

14  LIST  OF  ILLUSTRATIONS. 

Page. 

Fig.  135.  Section  near  mouth  of  Sandy  Creek,  Cheat  River,  Preston  Co.,  W.Va  ...  188 

136.  Section  on  Booth’s  Creek,  Taylor  Co.,  W.Ya 189 

137.  Section  under  Clarksburg,  W.  Ya 189 

138.  Section  near  Farmington,  W.  Va 189 

139.  Section  under  Wellsburgh,  W.  Ya 190 

140.  Section  in  Mercer  Co.,  Pa 190 

141.  Section  at  Ohio  and  Pennsylvania  line,  on  Mahoning  River 191 

142.  Section  in  Holmes  Co.,  Ohio 191 

143.  Section  of  Epler  oil  boring,  Washington  Co.,  Ohio 192 

144.  Section  under  Parkersburg,  W.  Ya 192 

145.  Section  at  Simpson  Well,  Wirt  Co.,  W.Ya 192 

146.  Section  at  Jackson  Furnace,  Jackson  Co.,  Ohio 193 

147.  Section  at  Hanging  Rock,  Scioto  Co.,  Ohio 193 

148.  Section  under  Big  Sandy  River,  at  mouth  of  Blaine  Creek 194 

149.  Section  under  Charleston,  Kanawha  Co.,  W.  Va 195 

150.  Section  at  Burning  Spring,  Kanawha  Co..  W.  Ya 196 

151.  Section  in  vicinity  of  Nuttallburgh,  Fayette  Co.,  W.  Ya 197 

152.  Section  on  Crane  Creek,  Mercer  Co.,  W.  Va 198 


LETTER  OF  TRANSMITTAL. 


Department  of  the  Interior, 

U.  S.  Geological  Survey, 

Appalachian  Division, 
Morgantown , W.  Va .,  July  15,  1890. 

Sir:  I have  the  honor  to  transmit  herewith  the  results  of  my  study 
of  the  stratigraphy  of  the  bituminous  coal  rocks  in  the  northern  half 
of  the  Appalachian  field. 

As  stated  in  the  body  of  this  report,  it  can  not  be  expected  that  this 
first  attempt  to  correlate  the  different  beds  of  coal,  limestone,  and  sand- 
stone over  such  a wide  area  will  be  free  from  error,  but  it  represents  * 
my  best  efforts  to  harmonize  the  strata  of  the  several  regions.  No 
one  knows  better  than  1 that  many  of  the  identifications  suggested  are 
largely  preliminary,  and  I not  only  expect  but  request  the  friendly 
criticism  of  my  brother  geologists,  knowing  that  all  will  be  pleased 
when  the  correct  order  of  these  interesting  deposits  shall  be  finally 
determined. 

Many  questions  of  great  geological  interest  have  not  been  discussed 
in  this  report,  for  the  reason  that  I thought  it  best  to  postpone  their 
treatment  until  some  one  should  have  done  for  the  southern  half  of  the 
Appalachian  coal  field  what  I have  attempted  for  the  northern  half, 
since  the  field  is  a unit  from  Pennsylvania  to  Alabama,  and  in  the  dis- 
cussion should  be  treated  as  such. 

It  is  hardly  necessary  to  say  that  the  accompanying  map  is  not  pre- 
sented with  any  claim  for  accuracy  as  to  details,  but  only  to  show  in  a 
rough  way  the  general  distribution  of  the  different  members,  and  with 
the  hope  that  it  may  prove  of  some  service  in  the  preparation  of  a cor- 
rect map  of  these  several  series  when  the  Survey  shall  have  extended 
"ts  topographic  work  over  the  entire  region. 

Very  respectfully,  your  obedient  servant, 

I.  C.  White. 

Hon.  J.  W.  Powell, 

Director  U.  S.  Geological  Survey , Washington , D.  C. 


15 


/ 


/ 


K 


Fig.  2 

izontal  Scale  36oooFT=I  inch, 
vtical  ” 36oo  ” 

ONS  ACROSS  THE  APPALACHIAN  COAL  FIELDS. 

, to  the  eastern  edge  of  the  Alleghany  Mountains. 

ihow  the  thickening  of  the  several  coal  groups  between  Jackson  County,  Ohio,  and  Fayette  County.  West 


I MILLERSBURG. 


CONG^JMEASURES 

SmLeVcZ. 


M E A S U 


UPPER  COAL  MEASURES. 


PERMO-CARB.  MEASURES. 


m 


PERMO-CARB.  measures 


Fig.  Z. 

Horizontal  Scale  36oooFT=I  inch, 
Vertical  " 36 oo  ” 


SECTIONS  ACROSS  THE  APPALACHIAN  COAL  FIELDS. 

?,  Ohio,  to  the  eastern  edge  of  the  Alleghany  Mountains. 


veen  Jackson  County,  Ohio,  and  Fayette  County.  West  'irginia. 


STRATIGRAPHY  OF  THE  BITUMINOUS  COAL  FIELD 
IN  PENNSYLVANIA,  OHIO,  AND  WEST  VIRGINIA. 


By  I.  C.  White. 


CHAPTER  I. 

AREA,  STRUCTURE,  AND  CLASSIFICATION. 

The  Appalachian  Basin  contains  the  largest  continuous  coal  field  of 
any  Carboniferous  area.  Beginniug  near  the  northern  line  of  Pennsyl- 
vania, latitude  42°,  longitude  77°,  it  extends  southwestward  through 
TVest  Virginia,  southeastern  Ohio,  eastern  Kentucky,  and  central  Ten- 
nessee, ending  in  western  Alabama,  latitude  33°,  longitude  88°,  900 
miles  from  its  northern  terminus. 

The  shape  of  the  field  has  been  compared  to  that  of  a rude  canoe 
the  poiu  ted  ends  being  in  Pennsylvania  and  Alabama,  respectively,  while 
the  broadest  portion  lies  in  southern  West  Virginia  and  Ohio. 

As  is  well  known,  the  general  structure  of  the  field  is  that  of  a great 
trough  or  basin,  the  line  of  greatest  depth  leaving  Pennsylvania  near 
its  southwest  corner,  and  passing  down  through  West  Virginia  rudely 
parallel  to  the  Ohio  River,  to  enter  Kentucky  10  miles  above  the  mouth 
of  the  Big  Sandy  River.  This  general  trough  or  geo-syncline  is  itself 
traversed,  especially  in  its  northeastern  portion,  by  a series  of  flexures 
which,  although  so  gentle  along  the  region  west  of  the  center  of  the 
field  as  to  be  recognizable  with  difficulty,  yet  eastward  thereof  they 
increase  in  amplitude  until  the  great  folds  of  the  Alleghany  Mountains 
become  a part  of  the  system. 

The  map  sections  shown  on  Pis.  X and  XI,  crossing  the  Appalachian 
held  nearly  normal  to  the  strike,  will  give  the  reader  a good  idea  of  the 
structure  of  the  northern  half  of  this  field  at  the  localities  indicated  on 
the  map  (PI.  I),  and  they  also  show  how  the  folds  which  are  so  promi- 
nent at  the  northeast  gradually  die  out  toward  the  southwest,  so  that 
in  the  region  ot  the  Great  Kanawha  River  they  almost  disappear.  This 
flattening  out  of  the  flexures  in  southern  West  Virgiuia  has  been 
ascribed  by  Professors  Fontaine  and  Stevenson  to  the  development  of 
the  great  system  of  faults  along  the  southeastern  margin  of  the  coal  field 
m the  edge  of  Virginia,  whicU  relieved  the  teusiou  ou  the  rocks  over 
Bull,  65 — 3 17 


18  THE  NORTHERN  BITUMINOUS  COAL  FIELD.  [buu.65. 

the  adjoining  portion  of  the  Appalachian  field  and  thus  prevented  their 
folding  as  in  Pennsylvania  and  northern  West  Virginia.  These  anti- 
clinal and  synclinal  folds  so  well  developed  at  the  north  are  nearly  par- 
allel .to  the  Alleghany  Mountains,  but  as  they  begin  to  die  away  in 
central  West  Virginia  a large  anticline  (the  Volcano)  runs  nearly  north 
and  south  diagonally  across  the  general  strike  of  the  beds. 

There  are  probably  other  folds  in  the  southwestern  part  of  West  Vir- 
ginia, which,  like  the  Volcano  anticline,  run  contrary  to  the  usual  direc- 
tion, but  they  have  not  been  traced  out  with  sufficient  care  to  warrant 
description. 

The  distribution  of  the  different  geological  groups  on  the  accompany- 
ing map  will  serve  to  show  the  general  position  and  direction  of  the 
principal  anticlines,  but  the  topographic  base  of  the  map  is  so  inaccu- 
rate that  it  was  thought  best  not  to  attempt  to  put  in  the  anticlinal 
lines  of  the  region  described  till  the  Survey  should  have  completed  the 
regular  topographical  map. 

In  this  connection  it  should  be  stated  that  this  map  is  not  presented 
with  any  claims  for  accuracy  in  detail,  but  simply  to  show  the  general 
distribution  of  the  Carboniferous  system. 

The  portion  of  the  Appalachian  region  herein  described  includes  only 
the  bituminous  coal  fields  of  Pennsylvania,  Ohio,  and  West  Virginia. 

The  Pennsylvania  and  Virginia  geologists,  led  by  the  two  illustrious 
Rogers  brothers,  long  ago  discovered  that  the  main  coal-bearing  portion 
of  the  Carboniferous  system  could  be  naturally  subdivided  into  five 
series.  This  generalization  was  founded  upon  a careful  study  of  the 
rocks  over  a wide  area,  and  the  subsequent  work  of  other  geologists  has 
fully  established  its  general  truthfulness  to  nature  as  well  as  its  great 
usefulness  in  stratigraphic  geology. 

The  more  detailed  and  minute  studies  of  recent  years,  rendered 
possible  by  vast  mining  developments,  have  only  modified  the  Rogers 
classification,  and  hence  it  has  become  so  thoroughly  ingrafted  into 
geological  nomenclature  and  so  familiar  to  the  minds  of  practical  coal 
operators  that  it  would  be  very  unwise  to  make  any  radical  changes  in  it. 
It  is  true  that  in  minor  details  the  original  nomenclature  for  some  of 
these  series  was  misleading,  but  this  does  not  materially  affect  the  grand 
truths  expressed  in  the  general  framework  of  the  classification,  and 
hence  it  has  been  deemed  best  to  modify  and  supplement  this  time- 
honored  work,  rather  than  to  destroy  it  and  cast  it  away,  as  has  recently 
been  suggested  by  some  geologists. 

The  classification  adopted  in  this  report  attempts  to  preserve  what- 
ever of  the  old  nomenclature  has  been  found  useful  and  helpful  to 
geologists,  while  at  the  same  time  such  new  features  are  introduced  as 
seem  necessary  from  our  wider  and  more  intimate  knowledge  of  these 

rocks.  J 

The  entire  Carboniferous  system  of  the  Appalachian  region  subdivides! 
naturally  into  three  grand  divisions  fouuded  upon  conditions  of  accu*J 


• HARMARVILLE  RO 
I ALLEGHANY  RIVER 


Horizontal  Scale  5 Miles=  I inch. 
Vertical  »5oooFT  » » 


SECTION  ACROSS  THE  APPALACHIAN  COAL  FIELDS,  FRO»<  RAVENNA,  OHIO,  TO  THE  ALLEGHANY  MOUNTAINS. 


WHITE.] 


DIVISIONS  OF  THE -CARBONIFEROUS  SYSTEM. 


19 


mulation,  and  these  in  turn  split  up  into  eight  minor  series,  as  exhibited 
in  the  following  scheme : 


Divisions. 


Upper:  fresh  and 
brackish  water 
deposits. 


Carboniferous  ^ Middle:  shore de- 
fcYSTEM posits,  with  in- 

cursions of  the 


Lower:  in  arine 
deposits. 


Series. 


Permo-Carboniferous,  No.  XYI,  Dunkard  Creek  Series. 


Upper  Coal  Measures,  No.  XV,  Monongaliela  River  Series. 

Upper  half. 


Barren  Measures,  No.  XIV,  Elk  River  Series. 


Lower  half. 


Lower  Coal  Measures,  No.  XIII,  Allegheny  River  Series. 


Pottsville  Conglomerate  Measures,  “Great,”  “Serai,”  No.  XII, 
Conglomerate,  etc. 


Mauch  Chunk  Red  Shale,  Umbral  Red  Shale.  'i 

Mountain  Limestoue,  Umbral  Limestone,  Green- >No.  XI. 
brier,  etc.  ) 


Pocono  Sandstone, Vespertine,  No.  X,  “Big  Injun  ” oil  sand,  etc. 


As  will  be  seen  from  the  foregoing  diagram,  the  line  between  the 
Middle  and  Upper  Carboniferous  deposits  passes  directly  through  the 
center  of  the  Elk  Biver  series.  This  is  due  to  the  fact  that  marine 
conditions  ceased,  never  to  return,  with, the  deposition  of  the  Crinoidal 
limestone  and  its  associated  beds,  midway  in  the  Barren  Measures, 
thus  separating  them  into  two  divisions  which  are  of  almost  equal  thick- 
ness, the  lower  one  abounding  in  marine  life,  while  the  upper  has  nothing 
but  fresh  or  brackish  water  forms.  The  change  in  this  respect  is  great 
enough  to  warrant  the  separation  of  the  Barrens  into  two  series,  but  as 
the  lithological  differences  at  the  line  of  separation  are  very  meager,  it 
is  deemed  best  to  keep  these  rocks  a unit  as  in  the  Bogers  nomenclature. 

This  report  deals  only  with  the  Middle  and  Upper  Carboniferous  of 
the  above  table,  and  the  five  series  into  which  they  are  subdivided  will 
now  be  described  in  detail,  beginning  with  the  highest. 

The  discussion  of  many  interesting  questions  connected  with  Carbon- 
iferous geology  is  necessarily  postponed  until  the  rest  or  southern  half 
of  the  Appalachian  coal  field  has  been  carefully  studied  as  a whole. 


CHAPTER  II. 


THE  PERMO-CARBONIFEROUS  OR  DUNKARD  CREEK  SERIES. 

THICKNESS,  CHARACTER,  AND  EXTENT. 

The  rocks  of  this  series  (Upper  Barren  Measures,  No.  XVI)  begin  with 
the  roof  shales  of  the  Waynesburg  coal  and  exteud  upward  to  the  top- 
most beds  of  the  Appalachian  region. 

How  many  feet  of  deposits  erosion  has  removed  above  the  highest 
remaining  beds  we  can  only  conjecture.  However,  if  the  soft  and  easily 
yielding  character  of  the  rocks  which  have  escaped  disintegration  can 
be  taken  as  a criterion  for  those  that  have  wasted  away,  the  thickness 
of  the  latter  must  be  reckoned  by  the  thousand  and  probably  by  the 
10,000  feet. 

Several  independent  measurements  from  the  highest  accessible  sum- 
mits foot  up  a little  more  than  1,150  feet  for  the  thickness  of  the  series 
and  it  is  certain  that  no  other  localities  could  exceed  this  by  more  than 
100  feet. 

The  uppermost  beds  are  found  at  the  headwaters  of  Dunkard  Creek, 
a large  stream  which  heads  near  the  West  Virginia-Pennsylvania  line, 
on  the  eastern  slope  of  the  watershed  separating  the  Ohio  and  Mono*n- 
gahela  River  drainage  system,  and  flowing  eastward  puts  into  the 
Monougahela  two  miles  above  Greensboro,  Greene  County,  Pennsyl- 
vania, and  four  miles  north  from  the  West  Virginia  line.  This  stream 
flows  over  Permo-Carboniferous  rocks  from  its  source  to  the  point  at 
which  it  leaves  the  West  Virginia  line  at  Mount  Morris,  Pennsylvania, 
a distauce  of  more  than  thirty  miles,  furnishing  very  fine  exposures  of 
these  rocks  along  its  banks  and  bluffs;  hence  the  geographical  name 
(Dunkard  Creek)  which  I have  given  the  series. 

These  deposits  occupy  a rather  limited  area  in  the  Appalachian  field, 
being  found  in  only  two  counties  (Greene  and  Washington)  of  Pennsyl- 
vania, with  the  exception  of  small  isolated  patches  in  Fayette,  West- 
moreland, and  Allegheny.  In  Ohio  there  is  a larger  area  of  them 
bordering  the  Ohio  River  through  the  counties  of  Belmont,  Monroe, 
Washington,  Athens,  Meigs,  and  Gallia.  But  it  is  in  West  Virginia 
that  we  find  the  principal  belt  of  these  beds,  for  there  they  cover  a wide 
20 


5EOLOGICAL  SURVEY 


PERMO-CARBONIFEROUS,  CAMERON,  WEST  VIRGINIA. 


Of  wt 


WWttW' 


Of  ILUHUVS 


WHITE.] 


CHARACTER  OF  THE  DUNKARD  CREEK  SERIES. 


21 


region  bordering  the  Ohio  River  between  the  Pennsylvania  line  at  the 
north  and  the  Great  Kanawha  River  on  the  south,  as  the  accompanying 
map  shows. 

The  character  of  the  rocks  varies  greatly  in  different  portions  of  this 
area.  At  the  northeastern  end  of  the  field,  in  Washington  County, 
Pennsylvania,  limestones  seem  to  predominate  in  thickness  over  the 
gray  shales,  sandstones,  and  thin  coal  beds  with  which  they  are  there 
interstratitied.  But  south  westward  the  limestones  and  coals  gradually 
disappear,  so  that  in  Jackson  County,  West  Virginia,  no  regular  coal 
beds  are  found,  and  only  one  limestone  (the  Nineveh)  remains.  The 
limestones  continue  in  considerable  number  in  Greene,  Ohio,  Marshall, 
and  Monongalia  Counties,  and  the  northern  part  of  Wetzel  County,  but 
southward  from  this  line  they  rapidly  disappear,  with  the  single  excep- 
tion noted.  The  coal  beds  all  die  out  with  the  disappearance  of  the 
limestones,  except  one  (the  Washington),  which  seems  to  extend  beyond 
the  Little  Kanawha  River  before  it  passes  out  of  the  series. 

As  the  limestones  and  thin  coal  beds  gradually  fade  out  to  the  south- 
west, red  shale,  a variety  of  rock  almost  unknown  in  Washington  County, 
Pennsylvania,  gradually  comes  into  the  section  in  thin  beds  at  first,  but 
finally  extends  throughout  the  whole  series,  and  forms  nearly  one-half 
its  thickness,  thus  making  a broad  band  of  red  soil  from  the  Pennsyl- 
vania line  southwestward  to  the  Great  Kanawha  River. 

This  increase  in  red  shale  beds  is  accompanied  by  an  increase  in  the 
number  and  massiveness  of  the  sandstone  rocks,  so  that  the  topography 
gradually  becomes  greatly  different  from  that  found  in  Washington 
County,  Pennsylvania.  There  the  surface  is  gently  rolling,  the  valleys 
broad,  and  the  hills  rounded,  with  no  deep  gorges  or  precipitous  slopes, 
the  abundance  of  limestone  rendering  the  soil  so  highly  fertile  that  the 
region  has  long  been  famed  as  one  of  the  finest  grazing  and  agricultural 
districts  in  the  Union.  But  toward  the  southwest,  while  the  soil  remains 
very  fertile,  owing  to  a large  quantity  of  marly  material  in  the  red 
shales,  yet  the  thickening  up  of  the  sandstone  beds  makes  the  valleys 
narrow  and  the  lower  portion  of  the  hills  often  precipitous,  the  arable 
land  being  confined  largely  to  the  ridges,  so  that  the  soil  is  better 
adapted  to  grazing  than  tillage.  In  many  cases  the  massive  sandstones 
crop  out  along  the  ridges  which  they  have  protected  from  erosion, 
forming  narrow  “ hogbacks,”  from  which  the  surface  falls  away  rapidly 
on  each  side.  Another  peculiarity  of  these  beds  is  that  the  sand  rocks 
contain  no  pebbles  except  near  the  base  of  the  series,  since  above  the 
Way nesburg  sandstone  no  pebbles  larger  than  coarse  sand  grains  have 
ever  been  seen  by  the  writer  in  all  of  the  1,000  feet  of  deposits,  except 
at  a single  locality  on  the  Parkersburg  and  Staunton  turnpike,  along 
the  dividing  ridge  between  Ritchie  and  Gilmer  Counties,  West  Virginia, 
where  locally  the  Marietta  Sandstones,  140  feet  above  the  Washington 
coal,  thicken  up  into  a very  coarse  conglomerate,  filled  with  quartz 
pebbles. 


1BE3HI 


22 


THE  NORTHERN  BITUMINOUS  COAL  FIELD. 


[BULL?  65. 


The  character  of  the  rocks  which  compose  these  measures  in  the  sev- 
eral regions  of  their  area  will  be  seen  from  the  sections 
which  follow. 

Section  on  Dunkard  Creek , Greene  County , Pennsyl- 
vania.— Fig.  1 shows  the  succession  found  along  Dunkard 
Greek,  from  £lie  head  of  its  Pennsylvania  fork  in  Gil- 
more Township,  Greene  County,  eastward  to  where  the 
stream  veers  northward  back  into  Pennsylvania  at 
Mount  Morris. 


Dunkard  Creek,  Greene  County,  Pennsylvania. 


I00- 


[See  map,  L 1 to  L Is.] 


Ft.  in. 


1.  Concealed  from  top  of  Shough’s 

knob 165 

2.  Sandstone,  massive,  Gilmore 40 

3.  Shales,  with  limestone  at  base  ...  15 

4.  Sandstone  and  shales  and  con- 

cealed   100 

5.  Shale,  red 2 

6.  Shales,  gray 20 

7.  Shale,  marly 2 

8.  Sandstone  aud  shale. 35 

9.  Shale,  red  3 

10.  Sandstone  and  shale 50 

11.  Red  shale  3 

12.  Shales  aud  sandstone,  Nineveh..  25 

13.  Shales  . 20 

14.  Coal,  Nineveh 1 6 

15.  Shales 28 

16.  Limestone  (No.  X),  Nineveh  7 

17.  shales,  sandstone  and  concealed.  100 

18.  Sandstone,  massive.  FishCreet..  20 

19.  Shales  with  fossil  plants 10 

t Joal. . 0-'  5"  ) 

20.  Coal,  Dunkard.  < Slate  O'  1"  > ..  1 

( Coal..  0'  6"  ) 

21.  Limestone 1 

•22.  Sandstone 10 

23.  Shales 17 

24.  Limestone,  Jolly  town 1 6 

25.  Shales  and  sandstone 25 

26.  Coal,  Jolly  town  1 1 

27.  Calcareous  shale,  fossiliferous, 

fish  teeth 0 6 

28.  Limestone.  Upper  Washington  ..  4 

29.  Shales  and  sandstone 115 

30.  Limestone,  Middle  Washington..  3 

31.  Shales 40 

32.  Sandstone 35 

33.  Shale... 5 


Cool  Wash  (Coal,  impure.  V 2") 

31-  . A F're  clay  ....  2'  6">  4 

ington  A.  }C()al  ._/ o'6"$ 

35.  Shales  and  sandstones 60 

36.  Limestone,  Lower  Washington  ..  5 

37.  Shales 5 

38.  Coal,  Washington,  slaty  5 

39.  Shales  and  sandstones,  including 

a coal  bed  near  center  110 

40.  Coal,  Waynesburg,  “A’’. 2 

41.  Shales 10 

42.  Sandstone,  Waynesburg 50 

43.  Shales,  with  fossil  plants  (Cass- 

ville) 5 

44.  Waynesburg  coal. 


> 


> 


) 


K 


) 


) 


Ft.  in. 


480 


223 


276  8 


182  6 


Total 


1,162  3 


Fig.  1.— Section  on  Dunkard  Creek,  Pa. 


WHITE.  ] 


SECTION  ON  COLVIN  S HUN,  PENNSYLVANIA. 


23 


Section  on  Colvin’s  Run , Greene  County , Pennsylvania . — The  lower  half 
of  this  Dunkard  Creek  series  is  very  finely  exposed  in  a continuous  sec- 
tion on  Colvin’s  Run,  a tributary  of  Dunkard  which  empties  into  it  near 
Mount  Morris,  Greene  County,  Pennsylvania,  and  in  descending  this 
stream  the  following  intervals,  as  shown  in  Fig.  2,  were  carefully  meas- 
ured : 


Ft.  in. 


> 190  6 


}■  245 

I 


Colvin’s  Bun,  Greene  County,  Pennsylvania. 

[See  map,  L 1.] 

Ft.  in. 

1.  Limestone,  Nineveh 9 

2.  Shales  and  sandstone 135 

3.  Limestone,  Jolly  town 10 

4.  Sandy  shales 35 

5.  Coal,  Jollytown  1 6 

6.  Shales,  sandy 35 

7.  Sandstone,  massive 15 

8.  Sandy  shales  and  concealed 40 

9.  Red  shales 10 

10.  Shales 25 

11.  Sandstone 10 

12.  Shales 15 

13.  Coaly  shales,  Washington,  “A” 2 

14.  Sandy  shales  and  sandstone 45 

15.  Limestone,  gray , 2 

16.  Shales 5 

17.  Sandstone,  massive 15 

18.  Shales 15 

19.  Limestone,  Washington  Lower 7 

20.  Shale,  dark 4 

21.  Coal,  Washington 2 6 

22.  Shales  and  sandstone 45 

23.  Coal,  Waynesburg,  “B’’ 2 

24.  Shales  and  sandstone 35 

25.  Limestone,  Colvin’s  Run 3 

26.  Shales 1 

27.  Coal,  Waynesburg,  “A” 2 

28.  Limestone 2 

29.  Shales 5 

30.  Sandstone,  Waynesburg I 75 

31.  Shales,  with  fossil  plants  (Cassville) 5 

32.  Coal,  Waynesburg. 

Total 613 


> 177  6 


Fig.  2. — Section  on  Col- 
vin’s Run,  Pa. 


24 


THE  NORTHERN  BITUMINOUS  COAL  FIELD. 


[bull.  65. 


Section  in  Aleppo  Township , Greene  County,  Pennsylvania. — Wheeling 
Creek  rises  on  the  western  slope  of  the  Monougahela-Ohio  divide,  and 
flowing  westward  enters  the  Ohio  River  at  Wheeling. 
It  furnishes  excellent  exposures  of  the  Dunkard  beds 
from  the  summit  of  the  series  to  the  base.  The  follow- 
ing intervals  (Fig.  3)  were  measured  along  the  Dunkard 
Fork  of  the  creek  between  its  source  in  Aleppo  Town- 
ship, Greene  County,  Pennsylvania,  and  the  mouth  of 
Crab  Apple  Creek,  near  the  West  Virginia  line: 


60' 


30 t 


wmm* 


Z!f 

pwi 

IS' 

— — 

6' 

40' 

1=:=.^=  = = 

gggggggj 

60’ 

10’ 

25* 

•Xv.V.v.v.v. 

mmWM 

65’ 

54 

,( 

HOT 

vt 

- ==J 

10' 

45' 

Aleppo  Township , Greene  County , Pennsylvania. 


[See  map,  L j.] 

Ft.  in. 

1.  Shales  and  sandstones 60 

2.  Limestone,  Windy  Gap  4 

3.  Shale 25 

4.  Coal  and  bituminous  shale. 

Windy  Gap 2 

5.  Shale 30 

6.  Sandstone,  Gilmore 30 

7.  Concealed  (shales,  sandstones, 

and  limestones) 300 

8.  Coal,  Nineveh 1 

9.  Shales 25 

10.  Limestone,  Xineveh 8 

11.  Shales  and  sandstone 40 

12.  Coal 1 2 

13.  Limestone 2 

14.  Sandstone 30 

15.  Limestone 8 

16.  Shales  and  sandstone 70 

17.  Limestone 2 

18.  Shale 15 

19.  Coal,  Dunkard 2 

20.  Limestone 1 6 

21.  Shaly  sandstone 25 

22.  Limestone,  Jollytown 2 

23.  Shales  and  sandstone 115 

24.  Dark,  calcareous  shale 2 

25.  Limestone 6 

26.  Shales  and  sandstone 40 

27.  Limestone 2 

28.  Shales  and  sandstone 60 

29.  Shales 10 

30.  Sandstone 25 

31.  Shales,  sandstones,  and  con- 

cealed  66 

32.  Coal,  Washington 4 

33.  Shales  and  concealed. 54 

34.  Coal,  Waynesburg,  “B” 1 

35.  Shales 24 

36.  Coal,  W ay nesburg,  “ A ’ ’ 0 

37.  Shales 10 

38.  Sandstone,  Waynesburg 45 

39.  Coal,  Waynesburg. 

Total 


Ft.  in. 


451 


} 232  8 


326 


]■  138 


1,147  8 


Fig.  3.  —Section  in  Greene  County,  Pa. 


WHITE.  1 


SECTION  AT  BOARD  TREE,  WEST  VIRGINIA. 


25 


3!j 


Section  at  Board  Tree  Tunnel , Marshall  County , West  Virginia. — At 
Board  Tree  Tunnel,  on  the  Baltimore  and  Ohio  Bailroad,  and  close  to 
the  line  between  Wetzel  and  Marshall  Counties,  some 
very  high  land  occurs,  while  an  oil  well  boring  in  the 
valley  of  Fish  Creek  near  by  carries  the  rock  meas- 
urement down  to  the  base  of  the  Dunkard  Creek  beds. 
In  descending  from  Bice’s  Knob  past  the  western  por- 
tal of  Board  Tree  Tunnel  to  the  Kuce  farm  oil  boring 
' on  Fish  Creek,  and  connecting  with  the  record  of  the 
latter,  the  following  succession  (Fig.  4)  is  revealed : 

Board  Tree.  Marshall  County , West  Virginia. 


t?.:v  iv.-::-:; 

is* 


100’ 


AOf 


26 1’ 


[See  map,  L j.] 

1.  Sandstone,  gray,  and  concealed*. 

2.  Gray  limestone,  Windy  Gap 

3.  Red  shales  and  concealed 

4.  Coaly  slate 

5.  Concealed  to  base  of  a massive 

sandstone 

6.  Concealed,  sandstone  and  red 

shale  to  Board  Tree  Tunnel 

7.  Sandy  shales 

8.  Sandstone,  Nineveh 

9.  Coal,  Nineveh 

10.  Gray  shales 

11.  Sandstone,  massive 

12.  Shales 

1'1 


13. 


150 


[Limestone 

C Limestone  ! Black  slate  . 

\ Nineveh  . ; Limestone  and 
limy  beds 

14.  Variegated  shales 

15.  Sandstone 

16.  Shales,  limy 

17.  Sandstone,  to  level  o£  track  at 

west  portal  

18.  Concealed  shales  and  sandstone. 

19.  Massive  sandstone,  Fish  Creek. 

20.  Shales  

21.  Coal,  Dunkard,  to  level  of  bore 

hole  

22.  Interval,  shales,  sandstones,  and 

limestones,  with  two  thin  coal 
beds 

23.  Shales,  sandstones,  and  red  beds. 

24.  Coal,  Washington  

25.  Shales, limestones, and  sandstone. 

26.  Coal,  Wayneshurg. 


Ft. 

55 

5 

100 

1 

35 

175 

15 

15 

1 

15 

12 

3 

19 

9 

5 

7 


100 

30 

3 


50 


150 


Ft. 


401 


} 261 


300 

155 


15!? 


Total 


1,117 


There  is  some  uncertainty  about  the 
horizon  of  the  Pittsburgh  coal  in  the 
oil  boring,  since  two  large  beds  are  re- 
ported, one  at  700  feet  and  the  other 
at  800.  The  latter  is  the  thicker  bed, 
and  as  the  depth  from  it  to  the  third  oil  sand  (2,100  feet)  agrees  with  the 


Fig.  4. — Section  at  Board  Tree  Tunnel,  Mar- 
shall Comity,  W.  Va. 


26 


THE  NORTHERN  BITUMINOUS  COAL  FIELD, 


[bull.  65. 


same  interval  15  miles  to  the  northeast,  I have  regarded  the  lower  bed  as 
the  Pittsburgh  in  constructing  the  above  section.  If,  however,  the  coal 
100  feet  higher  should  prove  to  be  the  Pittsburgh,  then 
the  5-foot  coal  150  feet  above  the  bottom  of  the  sec- 
tion would  probably  be  the  Waynesburg  bed,  and  the 
Dunkard  Greek  series  should  be  cut  off  just  above  it, 
and  thus  shortened  by  155  feet  at  this  locality. 

In  the  vicinity  of  Bellton,  Marshall  County,  West 
Virginia,  4 miles  west  from  Board  Tree  Tunnel,  the 
exposures  are  very  fine  and  the  surface  outcrops  can 
there  also  be  combined  with  the  record  of  an  oil  bor- 
ing, which  thus  gives  another  measurement  of  the  en- 
tire series. 

' Section  at  Bellton , Marshall  County , West  Virginia. — 
In  descending  from  the  highest  summits  near  Bellton, 
the  following  succession  (Fig.  5)  is  obtained  when 
combined  with  an  oil-boring  record  which  was  pub- 
lished by  the  writer  in  the  Annals  of  the  Lyceum  of 
Natural  History,  New  York,  July,  1874 : 

Bellton , Marshall  County , West  Virginia. 


35' 


284V  immmm 


;cv.\v,v 


[See  map,  Lj.] 

Ft.  Ft.  in 

1.  Limestone,  Windy  Gap 5 1 

2.  Shales  30 

3.  'Coal,  Windy  Gap,  blossom 0 

4.  Concealed  and  sandstone  and 

shales 30 

5.  Shales  and  sandstone 60 

6.  Sandstone,  massive,  gray 20  } 333 

7.  Ked  shales  and  concealed 75 

8.  Sandstone,  massive  40 

9.  Red  shales  and  sandstone.  50 

10.  Limestone 3 | 

11.  Shales  and  concealed 20 

12.  Coal,  Nineveh 1 

13.  Shales  and  sandstone 35 

14.  Limestone  and  shales,  Nineveh..  10 

15.  Shales,  sandstone  and  concealed.  100 

16.  Sandstone 5 

17.  Shales 10 

18.  Limestone 0 ( 

19.  Coal 0 ! 

20.  Shales  and  sandstone 15 

21.  Ked  shales 5 284  8 

•22.  Concealed 20 

23.  Coal 1 

24.  Shales  and  concealed 30 

25.  Coal, Dunkard- ^^5kslate1J'^  1 3 

26.  Limy  shales  and  fire  clay 5 

27.  Shales 13 

28.  Limestone,  gray,  Jollytown 2 

29.  Shales  and  sandstones 30 

30.  Coal,  Jollytown 0 8 J 

31.  Limestone,  gray,  Upper  Wash- 

ington (continued  from  oil- 
well  record) 5 ) 

32.  Sandstone 12 

33.  Shale - 7 

34.  Sandstone H 

35.  Shale 12 

36.  Fire  clay 7 

- 25 


37.  Sandstone 

38.  Shale 12 

39.  Sandstone 17 


Fig.  5. — Section  at  Bellton,  W.  Va. 


WHITE.] 


SECTION  AT  NEW  MARTINSVILLE,  W.  VA. 


2 7 


Ft.  in. 

40.  Coaly  shales  9 

41.  Sandstone 9 

42.  Shale 5 

43.  Sandstone 4 

44.  Shale 19 

45.  Sandstone 16 

46.  Shale 4 

47.  Sandstone, 30 

48.  Shale 2 

49.  Sandstone 35 

50.  Shale 27 

51.  Sandstone 45 

52.  Coal,  Washington 6 

53.  Sandstone 20 


Ft.  in. 


313 


Ft.  in. 


148 


> 148 


Ft.  in. 

54.  Limestone  8 

55.  Shale 19 

56.  Sandstone 15 

57.  Shale 18 

58.  Sandstone 25 

59.  Shale 4 

60.  Limestone 10 

61.  Fire  clay 3 

62.  Limestone 4 

63.  Sandstone 16 

64.  Place  for  Waynesburg 

coal. 


Total 1,078  8 


This  boring  did  not  reach  the  Pittsburgh  coal,  and  hence  the  identi- 
fication of  the  6-foot  coal  bed,  142  feet  above  the  base  of  the  section,  is 
made  on  the  same  basis  as  that  of  the  5-foot  bed  150 
feet  above  the  bottom  of  Section  4,  since  the  two  coals 
are  evidently  identical.  The  thin  coals  in  the  upper 
half  of  the  series  have  been  named  the  Bellton  group 
from  this  locality. 

Section  at  Neio  Martinsville,  West  Virginia. — In  pass- 
ing south  westward  from  this  area  of  maximum  devel- 
opment of  the  Permo-Carboniferous  rocks  a considerable 
change  takes  place  in  the  character  of  the  beds.  The 
Bellton  coal  group  practically  disappears,  and  also  many 
of  the  limestones,  so  that  in  the  vicinity  of  New  Martins- 
ville, Wetzel  County,  West  Virginia,  the  lower  half  of 
the  series  presents  the  structure  shown  in  Fig.  6 : 

Net v Martinsville , Wetzel  County,  West  Virginia. 

|See  map,  M i.] 


11 T* 


Ft. 

1.  Red  shale 

2.  Concealed 

3.  Red  shale 

4.  Limestone,  Nineveh,  in  several  layers  separated  by  shale 

5.  Red  marly  shale 

6.  Concealed  and  sandstone 

7.  Red  shale 

8.  Sandstone,  sandy  shales,  and  concealed 

9.  Red  shale 

10.  Sandstone,  massive.  

11.  Concealed 

12.  Red  shale 

13.  Concealed 

14.  Sandstone,  brown  massive 

15.  Sandy  shales 

16.  Red  shale _ 

17.  Sandstone 

18.  Red  shale  

19.  Sandstone  and  sandy  shales 

20.  Concealed  and  sandy  shales 

21.  Red  marly  shales,  with  limestone  nodules 

22.  Sandy  shale,  gray 

23.  Sandstone,  massive - 

24.  Sandy  shales 

25.  Red  shale  with  limestone  nodules 

26.  Shale,  gray,  sandy 

27.  Sandstone,  massive 

28.  Sandy  shales  

29.  Limestone,  impure 

30.  Sandy  shales  

31.  Coal,  Washington 4 

32.  Sandy  shales 5 

33.  Sandstone,  massive 35 

34.  Concealed  and  sandy  shales 25 

35.  Shales,  sandstones,  and  concealed 50 

36.  Waynesburg  coal. 

Total 


Ft. 

5 

45 

2 

10 

5 

30 

5 

30 

10 

10 

35 

5 

25 

10 

23 

2 

25 

5 

25 

20 

5 

15 

20 

15 

5 

2 

30 

3 

2 

20 


119 


563 


Fio  .6.— Section  at  New 
Martinsville,  W.  Va. 


28 


THE  NORTHERN  BITUMINOUS  COAL  FIELD. 


[BULL.  65. 


No.  4 appears  to  represent  the  Nineveh  limestone,  though  its  inter- 
val above  the  base  of  the  series  is  less  here  than  usual. 


Fig.  7. — Section  at 
.Baresville,  Ohio. 


Not  a single  one  of  the  Beliton  coals  was  observed  in 
this  section,  though  some  of  them  may  have  been  pres- 
ent and  concealed. 

(Section  at  Baresville , Ohio. — In  the  vicinity  of  Bares- 
ville,  Monroe  County,  Ohio,  a long  section  was  rnaile 
by  the  late  Prof.  E.  B.  Andrews.  It  is  referred  to  in 
vol.  II,  Ohio  Geology,  page  587,  and  published  on  Map 
XIII,  section  No.  II.  The  locality  is  only  1 J miles  above 
New  Martinsville,  West  Virginia,  and  the  succession 
reads  as  follows  (Fig.  7) : 

Baresville,  Monroe  County,  Ohio . 


[See  map,  M 1] 


1.  Coal,  blossom 

2.  Concealed  

3.  Limestone,  ineveli 

4.  Shale  . . 

5.  Limestone,  sandy 

6.  Red  shale  

7.  Shale,  mostly 

8.  Shale 

y.  Sandstone,  laminated  

10.  Red  shale  

11.  Sandstone 

12.  Red  shale - ... 

13.  Sandstone 

14.  Shale 

15.  Sandstone 

16.  Red  shale 

17.  Sandstone 

18.  Shale - 

19.  Sandstone 

20.  Shale 

21.  Coal,  blossom,  Jollytown 

22.  Shale  

23.  Sandstone  

24.  Sandy  shale 

25.  Sandstone 

26.  Shale  

27.  Sandstone 

28.  Shale  

29.  Sandstone 

30.  Shale 

31.  Sandstone 

32.  Shale 

33.  Sandstone 

34.  Shale 

35.  Sandstone  

36.  Shale - 

37.  Sandstone 

38.  Shale - 

( Coal.... O'  9"1 

39.  Coal,  Washington  “A  ’.  < Clay . . . O'  4"  S 

t Coal.... 2'  0"  > 

40.  Clay - 

41.  Shalle 

42.  Sandstone 

43.  Shale 

44.  Sandstone 

45.  Shale 

46.  Concealed 

47.  Sandstone,  Waynesburg 

48.  Shale 

49.  Coal,  Waynesburg. 

Total 


Ft.  in.  n 


6 

18 

2 

14 

21 

20 

36 

18 

2 

20 

3 

4 

3 
13 
11 

4 


3 


145 


201 


J 


3 

4 
13 

1 

12 

6 

4 

5 

5 > 149 

4 
23 
12 

3 
2 

28 

4 

20  j 

* 

3 1 


7 

2 

5 

1 

3 

15,6 

15 

3 


692  1 


WHITE.  ] 


SECTION  AT  WASHINGTON,  PA. 


29 


The  coal  blossom  at  the  summit  of  Section  7 appears  to  come  at  a 
horizon  above  any  of  the  Bellton  beds,  and  hence  is  a new  and  prob- 
ably extremely  local  element  in  the  series. 

Section  in  Liberty  Toicnship , Washington  County , 
Ohio . — The  following  (Fig.  8)  succession  of  the  beds 
in  the  lower  portion  of  this  series  is  reported  by  Mr. 
F.  W.  Minshall  from  a hill  near  the  Epler  oil  boring 
in  Liberty  Township,  Washington  County,  Ohio: 


IQ 


i40' 


Liberty  Township,  Washington  County,  Ohio 

[See  map,  M g.] 

1.  Shales  and  sandstones  • 

2.  Coal,  Jollytown  

3.  Shales  and  sandstone 1 

4.  Coal,  Washington  “A” 

5.  Shales  and  limestone 

6.  Sandstone 


8.  Ccal,  Washington 

9.  Limestone  and  shales 


12.  Waynesburg  coal. 
Total 


Ft. 

Ft. 

in. 

100 

1 

8 

140 

2 

6 

31  ) 

16  i 

59 

12  S 

1 

3 

66  ) 

28  > 

100 

6 J 

404 

5 

59' 


loo* 


big  ©. — Section  ill 
Washington  County, 
Ohio. 


These  identifications  are  made  on  the  supposition 
that  the  Macksburg  coal  of  the  Ohio  geologists  is  the 
equivalent  of  the  Waynesburg  bed. 

Section  at  Washington , Pennsylvania. — In  Washing- 
ton County,  Pennsylvania,  the  Dunkard  series,  as  al 
already  stated,  contains  much  more  limestone  than 
elsewhere,  and  the  intervals  between 
the  several  members  are  somewhat  less 
than  in  Greene  County.  The  following 
section  (Fig.  9)  from  Geological  Survey, 

Pennsylvania,  Report  K,  page  248,  ex- 
hibits the  structure  of  the  lower  portion 


of  these  beds  at  Washington,  Pennsylvania  : 


Washington,  Pennsylvania . 

[See  map.  J 1.] 


Ft.  in. 


Limestone,  Jollytown 

Shale  

Coal,  Jollytown 

Sandstone 10 

Dark  shale 8 

Limestone,  Upper  Washington  30 

Concealed  50 

Coal,  blossom 0 

Concealed  80 

Limestone,  Lower  Washington 12 

Coal,  Washington 7 

Clay  4 

Sandstone 9 

Concealed 10 

Limestone. 2 

Shales,  limestone,  and  concealed 65 

Black  slate 3 

Limestone 4 

Blue  shale  15 

Waynesburg  coal. 

Total 


Ft. 

10 


190 


S 117  0 


323  6 


Pig.  9. — Section  at 

Waelmigtou,  Ta, 


30  THE  NORTHERN  BITUMINOUS  COAL  FIELD.  [bull.  65. 

Section  near  Taylorstown , Pennsylvania. — Another  section,  from  the 
same  volume  page  259,  exhibits  the  succession  in  the  lower  half  of  this 
series  in  Buffalo  Township,  Washington  County,  Pennsylvania,  as 
shown  in  Fig.  10. 

In  both  these  sections  (9  and  10)  the  writer  has  changed  the  identi- 
fications of  some  of  the  beds  (notably  that  of  the  Jollytown  coal)  from 
that  made  in  the  original  sections  by  Stevenson,  but  in  every  such  case 
the  change  is  clearly  warranted,  since  the  coal  in  question  was  placed 
too  near  the  Washington  coal  by  Stevenson. 


Near  Taylorstown , Washington  County , Pennsylvania. 


[See  map,  J k.] 

Ft.  in. 

1.  Limestone,  in  fragments 

2.  Shales  and  sandstone 

3.  Coal,  blossom,  Jollytown 0 

4.  Shale 10 

5.  Limestone 6 

6.  Concealed 20 

7.  Limestone 12 

8.  Sandstone .. 15 

9.  Coal .* 0 8 

10.  Concealed 40 

11.  Limestone 15 

12.  Concealed 45 

13.  Limestone 10 

14.  Concealed 5 

15.  Coal 0 

16.  Concealed,  with  much  limestone 25 

17.  Coal,  Washington 6 

18.  Concealed,  with  a limestone 85 

19.  Coal,  blossom,  Waynesburg  “B  ” : 0 

20.  Concealed 40 

21.  Coal,  blossom,  Waynesburg  “A”  . 0 

22.  Waynesburg  sandstone 50 

23.  Shales 10 

24.  Coal,  Waynesburg 

Total 


Ft.  in. 

0 

40 

1 


> 203  8 


J 

1 

I 


0 


384  8 


The  very  highest  beds  of  the  Dunkard  Creek  series  known  to  the 
writer  occur  in  Shougli’s  Knob,  at  the  head  of  Dunkard  Creek,  Gilmore 
Township,  Greene  County,  Pennsylvania,  but  these  are  concealed  by  a 
thick  covering  of  soil,  and  hence  could  not  be  seen  in  detail.  The  high- 
est rock  of  the  series  which  has  been  traced  over  any  considerable  area 
is  the  Windy  Gap  Limestone. 

CHARACTERISTIC  HORIZONS. 


TIIE  WINDY  GAF  LIMESTONE. 

This  has  been  named  from  its  occurrence  near  Windy  Gap,  a “ divide  ” 
separating  the  Laurel  llun  branch  of  Fish  Creek  from  the  waters  of 
Wheeling  Creek,  in  Springhill  Township,  Greene  County,  Pennsylvania, 


WHITE.] 


CHARACTERISTIC  HORIZONS. 


31 


The  stratum  is  usually  of  a bluish  gray  color,  quite  pure,  and  has  a 
thickness  of  about  five  feet.  It  contains  minute  fresh  water  fossils, 
and  occasionally  small  crystals  of  blende. 

The  only  land  geologically  and  topographically  high  enough  to  catch 
this  stratum  is  that  which  clusters  about  the  southwestern  corner  of 
Pennsylvania,  in  Greene  County,  and  the  adjoining  regions  of  Mar- 
shall, Wetzel,  and  Monongalia,  in  West  Virginia.  Only  one  point 
(Hunsucker’s  Knob)  in  the  last  county  is  high  enough  to  catch  this 
limestone,  since  its  outcrop  ranges  between  1,500  and  1,600  feet  above 
the  sea.  The  sections  (Figs.  3 and  4)  at  Board  Tree  and  Bellton,  in 
Marshall  County,  as  well  as  the  one  (Fig.  2)  in  Aleppo  Township, 
Greene  County,  show  this  stratum  near  their  summits,  but  its  horizon 
is  concealed  in  Shough’s  Knob  of  the  Dunkard  Creek  section  (Fig.  1). 

This  is  the  same  stratum  as  that  numbered  Limestone  XIV  by  Prof. 
John  J.  Stevenson  in  his  Eeport  K,  Second  Geological  Survey  of  Penn- 
sylvania. 

THE  WINDY  GAP  COAL. 

At  an  interval  of  25  to  30  feet  below  the  limestone  just  described 
there  occurs  a small  coal  bed  just  under  the  summit  of  the  “ divide”  at 
Windy  Gap,  Greeue  County,  Pennsylvania,  and  it  has  been  designated 
from  that  locality.  Xo  opening  into  it  has  ever  been  made,  and  hence 
it  is  known  only  as  a blossom  which  exposes  one  to  two  feet  of  coal  and 
black  slate,  the  latter  filled  with  the  fossil  Cypris,  or  a closely  allied 
form. 

The  same  bed  was  also  seen  in  Aleppo  Township,  and  in  the  summit 
of  the  hills  at  Bellton.  It  is  the  highest  known  coal  of  the  series,  and 
comes  about  1,050  feet  above  the  Waynesburg  bed. 

* THE  GILMORE  SANDSTONE. 

Crowning  the  upper  portion  of  the  Permo-Carboniferous  beds  over  a 
considerable  area  around  the  heads  of  Dunkard,  Wheeling,  and  Fish 
Creeks,  there  occurs  a very  massive  sandstone  having  a thickness  of  25 
to  40  feet.  It  was  named  the  Gilmore  sandstone  by  Professor  Steven- 
son, from  its  occurrence  in  the  township  of  that  name  in  southwestern 
Greene  County.  This  stratum  is  usually  a coarse  and  very  massive 
sandstone,  excellent  for  building  purposes,  and  often  forming  long  lines 
of  cliffs  on  the  summits  of  the  high  ridges.  These  cliffs  are  always 
traversed  with  fissures,  and  they  furnish  a convenient  retreat  for  foxes 
when  chased  by  hounds,  so  that  the  stratum  in  question  is  often  locally 
known  as  the  u Fox  rocks,”  and  again  it  is  named  from  the  farms  where 
the  cliffs  occur,  as  “Pethtle”  rocks,  “ Efaw”  rocks,  etc.  This  stratum 
has  been  the  main  agency  in  preserving  all  of  the  very  high  beds  of 
the  Permo-Carboniferous  from  erosion. 

The  interval  below  the  Gilmore  sandstone  for  200  to  250  feet  consists 
of  red  shales,  occasional  thin  limestones,  and  gray  sandstones,  but  con- 


32 


THE  NORTHERN  BITUMINOUS  COAL  FIELD. 


[bull.  65. 


tains  no  beds  sufficiently  characterized  to  be  identifiable  over  any  con- 
siderable area. 

THE  NINEVEH  SANDSTONE. 

At  225  to  250  feet  below  the  Gilmore  sandstone,  we  come  to  another 
great  sandstone  deposit  which,  from  its  good  development  near  the  vil- 
lage of  Nineveh,  Greene  County,  Pennsylvania,  has  been  designated 
from  that  locality.  Like  the  Gilmore  sandstone  above,  it  is  usually 
an  excellent  building  stone,  and  has  long  been  used  for  that  purpose 
on  the  Baltimore  and  Ohio  .Railroad,  near  Littleton,  Wetzel  County, 
West  Virginia,  where  it  crops  out  in  a great  cliff  along  the  hills  150  to 
200  feet  above  creek  level. 

This  same  stratum  may  also  be  seen  in  the  hills  two  miles  above  Jol- 
lytown,  Greene  County,  where  it  has  long  been  quarried  on  the  land 
of  Thomas  White  for  building  purposes.  It  is  of  a yellowish  gray  cast, 
rather  coarse-grained,  but  soft,  and  splits  readily  into  rectangular 
blocks. 

THE  BELLTON  COAL  GROUP. 

At  275  to  300  feet  under  the  Gilmore  sandstone  we  find  the  upper- 
most of  a series  of  thin  coals  which,  from  their  fine  exposure  at  the  vil- 
lage of  Bellton,  Marshall  County,  West  Virginia,  have  been  termed  the 
Bellton  group.  These  coate,  few  of  which  are  rarely  more  than  one 
foot  thick,  occur  within  a rock  interval  of  200  to  300  feet,  and  when  all 
are  present,  as  in  the  Bellton  section  (Fig.  5),  there  are  five  distinct  beds, 
though  not  all  of  them  are  persistent  over  auy  considerable  area.  The 
three  beds  given  in  the  Dunkard  Creek  section  (Fig.  1),  viz,  the  Nine- 
veh, Dunkard,  and  Jolly  town  coals,  are  the  most  important  members 
of  the  group.  Interstratified  with  these  coals  are  shales^  sandstones, 
and  two  important  limestones. 

THE  NINEVEH  COAL. 

This  is  the  uppermost  member  of  the  Bellton  group,  and  was  named 
from  the  village  of  Nineveh,  Greene  County,  Pennsylvania,  by  Professor 
Stevenson. 

The  coal  rarely  exceeds  one  foot  in  thickness,  yet  it  is  generally  quite 
pure,  and  is  frequently  used  for  smithing  purposes. 

In  the  hills  at  Bellton  it  crops  out  290  feet  above  Fish  Creek,  and  the 
same  coal  is  seen  in  the  railroad  cut  at  the  western  portal  of  Board 
Tree  Tunnel,  75  feet  above  track  level. 

On  the  head  waters  of  Dunkard  Creek  it  is  known  as  the  John  Tay- 
lor coal,  and  although  only  one  foot  thick  is  highly  valued  as  a smithing 
fuel. 

THE  NINEVEH  LIMESTONE. 

Below  the  Nineveh  coal  at  an  interval  of  25  to  30  feet  there  comes  a 
limestone  which  has  a very  extended  distribution.  It  was  called  Lime- 
stone No,  X by  Professor  Stevenson  in  his  .Report  K,  Greene  and  Wash- 


WHITE.] 


CHARACTERISTIC  HORIZONS. 


33 


ington  Counties,  but  itis  here  designated  from  the  same  village  in  Greene 
County  which  has  given  name  to  the  coal  and  sandstone  already  de- 
scribed. 

This  limestoue  usually  consists  of  several  layers  separated  by  shales 
the  whole  of  which  sometimes  foots  up  nearly  20  feet,  as  in  the  section 
at  Board  Tree  Tunnel  (Fig.  4),  but  its  usual  thickness  is  seldom  more 
than  10  feet.  Frequently  a stratum  of  bituminous  shale  is  found  inter- 
stratified  with  the  layers  of  limestone.  Some  of  the  latter  are  quite 
pure,  and  furnish  excellent  lime.  It  has  a very  wide  distribution,  as 
may  be  seen  from  its  presence  in  each  of  the  first  seven  sections  already 
given.  The  same  stratum  extends  clear  through  to  Jackson  County, 
West  Virginia,  and  nearly  to  the  Big  Kanawha  Biver,  where  it  occurs 
high  up  on  the  summits  of  the  hills  and  is  hence  termed  the  “ Ridge  v 
limestone,  by  the  farmers. 

There  is  a fine  exposure  of  this  rock  at  Limestone  Hill  Post-office,  on 
the  Parkersburg  and  Charleston  turnpike,  near  the  corners  of  Wirt, 
Wood,  and  Jackson  Counties, West  Virginia.  It  is  there  nearly  30  feet 
thick,  in  several  layers,  and  contains  many  minute  fossils,  all  apparently 
of  fresh- water  types. 

THE  HOSTETTER  COAL. 

Occasionally  a bed  of  coal  occurs  at  75  to  100  feet  below  the  Nineveh 
limestone.  It  has  been  stripped  out  of  the  run  on  the  old  Hostetter 
farm  near  Burton,  Wetzel  County,  West  Virginia,  where  it  is  12  to  15 
inches  thick  and  rather  pure.  It  also  appears  to  be  present  in  some 
localities  near  the  head  of  Dunkard  Creek,  and  in  a local  section  near 
Bellton  it  was  seen  15  inches  thick  at  130  feet  below  the  Nineveh  coal. 

THE  FISH  CREEK  SANDSTONE. 

At  135  to  150  feet  below  the  Nineveh  coal,  there  often  occurs  a very 
massive  sandstone.  It  makes  the  great  cliffs  along  the  waters  of  Fish 
Creek  in  Springhill  Township,  Greene  County,  Pennsylvania,  and  was 
designated  from  this  stream  by  Stevenson  in  his  Report  K. 

The  rock  in  question  is  frequently  quite  massive,  and  it  makes  an  ex- 
cellent building  stone.  It  is  very  conspicuous  in  the  region  of  Deep 
Valley,  Pennsylvania,  where  it  forms  long  lines  of  vertical  cliffs  25  to 
30  feet  high.  It  may  also  be  seen  in  cliffs  along  the  Baltimore  and  Ohio 
Railroad,  above  Littleton,  in  Wetzel  County,  where  it  is  quarried  for 
building  purposes. 

THE  DUNKARD  COAL. 

Below  the  Fish  Creek  sandstone,  at  an  interval  of  1 to  20  feet,  another 
coal  bed  is  often  found,  which,  from  its  occurrence  along  the  bed  of 
Dunkard  Creek  for  a considerable  distance,  was  named  the  Dunkard  coal 
by  Professor  Stevenson.  It  is  seldom  more  than  12  to  15  inches  thick, 
but  is  almost  invariably  double,  having  a thin  layer  of  slate  near  its 
Bulk  05 3 


34 


THE  NORTHERN  BITUMINOUS  COAL  FIELD. 


^BULL.  65. 


center.  At  Deep  Valley,  Pennsylvania,  however,  this  parting  thick- 
ens up  to  five  feet  or  more  aiul  thus  separates  the  coal  into  two  well- 
defined  beds,  each  of  which  is  8 to  10  inches  thick.  In  the  roof  shales 
of  this  coal  at  Mr.  Lee  Garrison’s,  in  Gilmore  Township,  Greene  County, 
Pennsylvania,  finely  preserved  fossil  plauts  abound,  principally  of  the 
genera  Neuropteris  and  Odontopteris. 

This  bed  is  frequently  stripped  along  the  streams  for  local  use  in 
Greene,  Monongalia,  Wetzel,  and  Marshall  Counties. 

THE  JOLLYTOWN  LIMESTONE. 

Below  the  Dunkard  coal,  at  an  interval  of  25  to  30  feet,  there  occurs 
a bed  of  limestone  which  is  rather  persistent.  It  is  well  exposed  in  the 
vicinity  of  Jollytown,  Greene  County,  Pennsylvania,  and  has  been  des- 
ignated from  that  locality.  As  may  be  seen  from  its  presence  in  Sec- 
tions 1 to  5 and  also  in  9,  this  limestone  has  a wide  distribution,  though 
at  the  head  of  Dunkard  (Fig.  1),  and  on  Fish  Creek  (Fig.  5),  the  stratum 
is  only  1 to  2 feet  thick.  In  Washington  County,  Pennsylvania,  how- 
ever, it  thickens  up  to  10  feet  or  more  and  is  usually  a rather  pure  lime- 
stone. 

THE  JOLLYTOWN  COAL. 

This  is  the  lowest  member  of  the  Bellton  coal  group,  and  underlies 
the  Jollytown  limestone  by  an  interval  of  25  to  30  feet.  The  coal  was 
named  by  Professor  Stevenson  from  a village  in  Greene  County,  Penn- 
sylvania. 

This  is  the  only  coal  of  the  Bellton  group  that  ever  attains  dimen- 
sions of  2 to  3 feet,  and  can  therefore  be  mined  by  drifting,  since  in 
the  vicinity  of  Wise,  Monongalia  County,  West  Virginia,  and  below 
this  along  the  South  Fork  of  Dunkard  Creek,  it  is  nearly  3 feet  thick, 
and  is  mined  to  a considerable  extent  for  local  use.  The  coal  is  not 
very  pure,  but  in  the  absence  of  any  other  beds  it  finds  a ready  market. 
In  the  Bellton  section  (Fig.  5)  this  coal  has  been  identified  with  the 
lowest  bed  exposed  there.  This  is  only  a few  inches  thick  and  quite 
slaty,  so  that  it  is  possible  the  Jollytown  bed  is  the  one  next  above,  and 
which  in  that  section  has  been  referred  to  the  Dunkard  coal. 

Along  Dunkard  Creek  the  Jollytown  coal  is  nearly  always  present, 
and  seldom  less  than  1 to  2 feet  thick.  It  becomes  a very  important 
key  rock  over  a wide  region,  since  there  are  seldom  any  other  coals 
below  it  for  an  interval  of  250  feet.  It  extends  almost  without  a break 
across  Greene,  Monongalia,  Marion,  and  Harrison  Counties,  but  appears 
to  thin  away  in  Doddridge. 

Throughout  Monongalia,  Greene,  and  Marshall  Counties,  the  interval 
between  this  bed  and  the  Washington  coal  below  is  about  275  feet, 
but  westward,  in  Washington  County,  Ohio  (Section  8),  the  interval 
thins  away  to  200  feet,  and  practically  the  same  measurement  is  found 
in  Washington  County,  Pennsylvania  (Sections  9 and  10). 


WHITE.] 


CHARACTERISTIC  HORIZONS. 


35 


THE  UPPER  WASHINGTON  LIMESTONE. 

Three  limestones  were  named  from  Washington,  Pennsylvania,  by 
Professor  Stevenson — an  Upper,  Middle,  and  Lower  one — and  two  of 
these  are  shown  in  the  section  (Fig.  9)  from  the  typical  locality. 

The  Upper  Limestone  is  a very  important  bed  in  Washington  County, 
since  it  has  a thickness  of  20  to  30  feet,  and  is  generally  very  pure.  It 
is  usually  of  a dark  blue  color,  and  is  much  used  for  macadamizing 
roads  and  burning  for  agricultural  and  other  purposes.  This  rock  ap- 
pears to  be  identical  with  the  limestone  seen  in  the  bed  of  Dunkard 
Creek  near  the  mouth  of  Negro  Bun,  above  Jolly  town,  Greene  County, 
Pennsylvania,  where  it  carries  a bituminous  shale  on  its  top,  filled  with 
fish  remains  and  other  minute  fossils,  and  underlies  the  Jollytown  coal. 

In  the  bed  of  Fish  Creek  at  Bellton,  Marshall  County,  TVest  Virginia, 
we  find  a limestone  with  a fish  bed  on  its  top,  which  appears  to  be  iden- 
tical with  the  Upper  Washington  deposit. 

THE  MIDDLE  WASHINGTON  LIMESTONE. 

About  midway  in  the  interval  between  the  Upper  Washington  lime- 
stone and  the  Washington  coal  there  is  frequently  found  another  lime- 
stone bed.  It  is  very  persistent  in  Washington  County,  Pennsylvania, 
and  is  often  15  to  20  feet  thick  and  of  a huffish  color. 

On  Dunkard  Creek  it  appears  to  be  represented  by  a stratum  seen 
just  above  the  road  at  Kent’s  Mills,  where  it  is  only  three  feet  thick. 
This  limestone,  like  all  of  those  in  the  Dunkard  series,  contains  minute, 
undetermined  fossils,  and  the  bituminous  shales  accompanying  them 
hold  plenty  of  fish  scales,  teeth,  etc.,  as  well  as  fragments  of  plants. 

WASHINGTON  “a”  COAL. 

At  70  to  80  feet  above  the  Washington  coal,  there  occurs  a bed  of 
impure  coal  and  coaly  shale- which  is  often  present  in  the  section  along 
Dunkard  Creek.  Sometimes  the  ehtire  bed  is  four  to  five  feet  thick, 
but  little  of  it  is  ever  merchantable  coal,  being  seldom  more  than  a 
bituminous  slate.  It  is  well  exposed  in  the  hills  about  Blacksville, 
and  Brownsville,  in  Monongalia  County,  and  there  contains  many  bi- 
valve crustaceans. 

Bituminous  shale  is  often  found  at  this  horizon  in  Washington  and 
Greene  Counties,  Pennsylvania,  and  in  Washington  County,  Ohio  (Fig. 
8),  a coal  bed  2J  feet  thick  seems  to  occur  at  the  same  place  in  the  series. 

THE  MARIETTA  SANDSTONES. 

The  Washington  “A”  coal  is  often  absent,  and  the  portion  of  the 
series  for  100  to  125  feet  above  the  Washington  coal  is  then  frequently 
occupied  by  two  or  three  beds  of  massive  sandstone.  These  crop  out 
in  the  hills  below  Marietta,  Ohio,  where  they  have  long  been  exten- 
sively quarried  for  grindstones  and  building  stone,  and  they  have  been 


36 


THE  NORTHERN  BITUMINOUS  COAL  FIELD. 


[bull.  65. 


designated  from  that  locality.  There  are  often  three  of  them,  each  25 
to  40  feet  in  thickness,  and  separated  by  thin  shales,  so  that  in  such 
cases  they  might  be  called  the  Upper,  Middle,  and  Lower  Marietta 
sandstones.  Sometimes,  however,  as  near  Bock  Lick,  Marshall  County, 
West  Virginia,  the  shales  thin  out  and  let  all  of  the  sandstones  coalesce 
into  one  mass  more  than  100  feet  thick. 

These  beds  form  the  great  cliffs  at  Eaven  Eock,  Pleasants  County, 
West  Virginia.  The  upper  one  is  extensively  quarried  at  the  Jackson 
quarry  in  Parkersburg,  West  Virginia,  and  it  with  its  associated  rocks 
forms  long  lines  of  cliffs  up  the  Little  Kanawha  Eiver,  where  they  have 
been  extensively  quarried  in  the  vicinity  of  Elizabeth  and  other  points. 

It  is  one  of  these  beds  that  makes  the  big  cliffs  on  the  hill  above  the 
famous  McGugan  gas  well  in  Washington  County,  Pennsylvania. 
These  rocks  are  sometimes  gray,  but  more  frequently  of  a yellowish  or 
huffish  cast,  and  moderately  coarse  in  grain.  They  also  occur  in  Bitch  ie? 
Wirt,  Jackson,  and  Putnam  Counties,  West  Virginia,  where  they  cap 
the  narrow  ridges  in  long  lines  of  cliffs. 

In  Greene  and  Washington  Counties,  Pennsylvania,  and  Monongalia 
County,  West  Virginia,  this  interval  of  100  feet  above  the  Washington 
coal  is  generally  occupied  by  shales,  limestones,  and  thin,  sandy  beds, 
massive  sandstones  being  exceptional. 

THE  BLACKSVILLE  LIMESTONE. 

In  some  portions  of  Washington,  Greene,  and  Monongalia  Counties, 
a limestone  occurs  with  considerable  persistency  at  30  to  50  feet  above 
the  Washington  coal.  This  was  numbered  Limestone  III  by  Professor 
Stevenson  in  his  Greene  and  Washington  report,  but  as  it  comes  to  the 
surface  near  the  bed  of  Dunkard  Creek,  in  the  village  of  Blacksville, 
Monongalia  County,  West  Virginia,  it  has  been  given  a geographical 
name  from  that  locality.  The  rock  is  generally  gray,  quite  pure,  and 
only  three  to  five  feet  thick.  It  is  seen  in  Section  2 at  46  feet  above 
the  Washington  coal.  It  soon  disappears  southward  from  the  Pennsyl- 
vania line. 

THE  LOWER  WASHINGTON  LIMESTONE. 

At  Washington,  Pennsylvania,  a limestone  of  unusual  thickness  (20 
feet)  forms  the  roof  of  the  Washington  coal,  and  it  was  designated,  from 
that  locality,  the  Lower  Washington  limestone  by  Stevenson.  It  has 
a wide  distribution  in  Greene,  Washington,  Ohio,  Belmont,  Marshall, 
and  Monongalia  Counties,  but  disappears  southward  from  these.  It 
often  attains  a thickness  of  20  to  30  feet  in  Washington  County,  but  is 
always  interstratified  with  much  shale,  and  outside  of  Washington 
County  is  seldom  more  than  5 to  10  feet  thick.  Frequently  some  of  the 
layers  contain  so  much  carbonate  of  iron  as  to  prove  a fair  ore.  These 
iron-bearing  layers  are  often  interstratified  with  bituminous  shales,  and 
in  such  cases  tbe  iron  layers  are  covered  with  fossil  plants.  It  is  on 


WHITE.] 


CHARACTERISTIC  HORIZONS. 


37 


these  thin,  shaly  layers  of  carbonate  of  iron  in  the  roof  of  the  Washing- 
ton coal  at  Brown’s  Bridge,  Dunkard  Creek,  on  the  West  Virginia- 
Pennsyl vania  line,  that  the  Permian  plant,  Callipteris  conferta , occurs 
as  described  in  Report  PP,  Second  Geological  Survey,  Pennsylvania, 
page  54. 

THE  WASHINGTON  COAL. 

This  bed,  which  is  the  only  one  in  the  Dunkard  series  that  is  worka- 
ble over  a wide  area,  was  first  described  by  the  writer,  and  named  the 
Brownsville  coal  from  its  occurrence  at  the  village  of  that  name  in 
Monongalia  County,  West  Virginia.  Subsequently,  however,  the  same 
coal  was  found  in  greater  development  at  Washington,  Pennsylvania, 
and  it  was  designated  from  that  locality  by  Professor  Stevenson. 

It  is  always  a multiple  bed,  being  separated  into  two  or  three  layers 
by  divisions  of  slate.  Occasionally  these  divisions  are  numerous  and 
the  entire  thickness  of  the  bed  is  8 to  10  feet, -but  in  all  cases  the  only 
pure  or  merchantable  coal  is  the  bottom  portion, which  seldom  exceeds 
two  and  a half  to  three  feet.  The  upper  part  of  the  bed  is  nearly 
always  very  impure,  since  it  contains  so  much  ash  and  slate  as  to  consti- 
tute it  a mere  bed  of  richly  bituminous  shale. 

This  coal  is  much  more  persistent  than  any  other  coal  of  the  Permo- 
Carboniferous  series,  since  it  occurs  everywhere  in  the  northern  area  of 
these  rocks,  and  does  not  disappear  to  the  southwest  except  beyond  the 
Little  Kanawha  River,  in  West  Virginia,  while  in  Ohio  it  seems  to  be 
persistent  even  to  the  southwestern  margin  of  these  deposits.  In  Wash- 
ington and  Meigs  Counties,  Ohio,  it  is  frequently  referred  to  by  Pro- 
fessor Andrews  as  the  Hobson  coal. 

(Section  at  Farmington , Marion  County , West  Virginia . — The  following 
section  of  this  coal,  taken  near  Farmington,  Marion  County,  West  Vir- 
ginia, well  illustrates  the  structure  of  the  bed  when  it  is  thick : 


1. 

2. 

3. 

4. 

5. 

6. 

7, 

8. 

9. 

10. 

11. 

12. 

13. 

14. 


Coal 

Shale 

Coal  and  shale 

Coal 

Shale  

Coal 

Shale 

Coal 

Shale 

Coal 

Shale 

Coal,  fair 

Slate 

Coal,  good 


Ft.  in. 
. 0 6 
. 0 3 
. 0 8 
. 1 0 
. 0 4 
. 0 5 
. 0 3 
. 1 0 
. 0 4 
. 1 1 
. 0 3 
. 2 0 
. 0 2 
. 2 6 


1 


4 


in. 


n 


Ft.  in. 
>10  9 

8 


Here  the  upper  or  roof  portion  of  the  coal,  although  0 feet  thick,  is 
entirely  worthless,  and  the  only  really  good  coal  in  the  bed  is  the  2£ 
feet  at  the  bottom. 


38 


THE  NORTHERN  BITUMINOUS  COAL  FIELD. 


[bull.  65. 


Through  Washington  County,  Pennsylvania,  this  coal  has  a thick- 
ness of  5 to  6 feet,  but  very  little  of  it  is  merchantable. 

It  is  frequently  exposed  along  the  Ohio  River  hills  between  Wheel- 
ing and  Parkersburg,  being  at  low  water  in  the  latter  town. 

Before  disappearing  to  the  southwest  it  dwindles  down  in  thickness 
very  much,  since  at  Harrisville,  Ritchie  County,  it  is  only  2 feet 
thick,  and  at  the  Grahamite  mines,  near  Hughes  River  in  the  same 
county,  only  feet. 

It  is  mined  for  local  supply  in  the  vicinity  of  Smith ville,  Ritchie 
County,  where  it  is  only  15  inches  thick  and  150  feet  above  the  level 
of  Hughes  River. 

Section  on  Willey  Fork,  Wetzel  County,  West  Virginia. — At  the  mouth 
of  the  Willey  Fork  of  Fishing  Creek,  Wetzel  County,  West  Virginia, 
this  coal  is  brought  a few  feet  above  water  level  by  a low,  anticlinal  roll, 
and  there  it  exhibits  the  following  structure : 


1.  Dark  shales  

2.  Coal 

3.  Coaly  shale 

4.  Shale,  gray,  sandy 

5.  Coal 

6.  Gray  shales *, 

7.  Coal,  slaty 


Ft. 

in. 

0 

5 " 

1 

6 

2 

0 

0 

3 

. 2 

0 

2 

0 j 

Section  near  Brown’s  Mills , Monongalia  County , West  Virginia. — Rear 
Brown’s  Mills,  Monongalia  County,  where  this  coal  was  first  described, 
it  has  the  following  structure: 

Ft.  in. 


1.  Bituminous  shale 

2.  Coal,  impure 

3.  Shale 

4.  Coal,  slaty 

5.  Shale 

6.  Coal,  good 


2 0 


1 4 
0 3 

2 4 > 


Ft. 

8 


At  this  locality  the  Lower  Washington  limestone  forms  the  roof 
above  the  bituminous  shale  Ro.  1,  and  it  also  contains  much  iron. 

Occasionally  a thin  coal  is  found  resting  immediately  on  top  of  the 
Lower  Washington  limestone,  and  that  condition  of  affairs  exists  at 
Brown’s  Mills,  where  a bed  of  coal  and  black  slate,  in  all  2 feet  thick, 
occurs  10  feet  above  the  top  of  the  Washington  coal.  The  bed  is  not 
persistent  enough  to  merit  a separate  name,  however. 


THE  WASHINGTON  SANDSTONE. 


Very  frequently  no  fire  clay  is  present  under  the  Washington  coal, 
and  the  latter  rests  directly  upon  a flaggy  sandstone,  often  finely 
laminated,  brown,  micaceous,  and  containing  vegetable  fragments  in 
great  quantity.  This  stratum, which  was  called  the  Washington  sand- 


WHITE.  ] 


CHARACTERISTIC  HORIZONS. 


39 


stone  by  Professor  Stevenson,  occurs  over  a wide  area  in  Monongalia, 
Greene,  and  Washington  Counties,  but  is  not  persistent  very  far  south 
of  the  Pennsylvania  line. 

THE  LITTLE  WASHINGTON  COAL. 

Just  under  the  Washington  sandstone,  and  10  to  20  feet  below  the 
Washington  coal,  there  sometimes  occurs  a thin  bed  of  coal,  seldom  at- 
taining afoot  in  thickness.  It  is  more  persistent  in  Washington  County, 
Pennsylvania,  than  elsewhere,  and  hence  was  designated  as  above  by 
Stevenson.  It  is  seldom  seen  south  from  the  Pennsylvania  line,  and  in 
Greene  County  even  is  represented  only  by  a thin  bed  of  bituminous 
slate. 

THE  WAYNESBURG  “b”  COAL. 

Below  the  last  little  coal  bed  there  usually  occur  shales,  thin  sand- 
stones, and  occasionally  a limestone,  down  to  about  45  feet  below  the 
Washington  coal,  where  another  small  bed  is  found  quite  persistent  in 
Monongalia,  Greene,  and  Washington  Counties.  It  is  seldom  more  than 
a foot  thick,  but  sometimes  attains  to  two.  It  has  never  been  seen  south 
of  Monongalia  County,  and  is  of  little  economic  importance. 

THE  COLVIN,S  RUN  LIMESTONE. 

Below  the  last  coal  come  30  to  35  feet  of  shale  and  thin  sandstones, 
and  then  we  get  a limestone  that  was  numbered  Limestone  1(a)  by 
Professor  Stevenson,  but  I have  given  it  the  above  geographical  desig- 
nation from  its  occurrence  at  the  locality  of  Section  2,  where  it  is  3 
feet  thick  and  quite  pure.  It  is  often  of  a bullish  cast,  however,  and 
contains  too  much  iron  to  slake  well  on  burning.  In  Washington 
County,  Pennsylvania,  this  stratum  thickens  up  to  8 and  10  feet,  but  it 
is  seldom  seen  south  of  the  Pennsylvania  line. 

THE  WAYNESBURG  “a”  COAL. 

This  occurs  just  under  the  last  mentioned  limestone  and  like  it  is  con- 
fined to  the  northern  end  of  the  Permo-Carboniferous  area.  It  some- 
times attains  a thickness  of  3 and  4 feet,  but  is  generally  slaty  and 
worthless,  so  that  it  has  seldom  been  mined.  It  occurs  quite  generally 
across  Monongalia,  Marion,  and  Harrison  Counties,  and  is  possibly 
present  in  Ritchie  County  near  Harrison ville,  but  beyond  that  it  has  not 
been  identified.  Its  horizon  is  usually  GO  to  80  feet  above  the  Waynes- 
burg  coal  proper. 

THE  MOUNT  MORRIS  LIMESTONE. 

Separated  from  the  coal  last  described  by  only  2 to  5 feet  of  clayey 
shales  there  sometimes  occurs  a limestone  which,  although  noted, 
was  not  named  by  Stevenson  in  his  Report  K.  It  is  well  exposed  on 
the  north  bank  of  Dunkard  Creek  at  Mount  Morris,  Greene  County, 
Pennsylvania,  and  has  been  designated  from  that  locality.  The  stratum 


40 


THE  NORTHERN  BITUMINOUS  COAL  FIELD. 


[bull.  65. 


is  often  only  1 to  2 feet  thick,  and  seldom  more  than  5 feet  except 
in  Washington  County,  Pennsylvania,  where  it  is  occasionally  thicker. 

This  limestone  is  not  persistent,  and  is  seldom  found  south  of  the 
Pennsylvania  line,  being  frequently  absent  even  in  Greene  and  Wash- 
ington Counties. 

THE  ,WAYNESBURG  SANDSTONE. 

Just  under  the  horizon  of  the  Mount  Morris  limestone,  and  separated 
from  it  by  2 to  5 feet  of  shales  and  clay,  there  comes  a very  im- 
portant sandstone.  This  was  long  ago  termed  the  Waynesburg  sand- 
stone, from  its  fine  development  near  the  town  of  that  name  in  Greene 
County,  Pennsylvania.  It  is  one  of  the  most  persistent  members  of  the 
Permo-Carboniferous  series,  since  its  eastern  outcrop  can  be  followed 
in  an  almost  constant  line  of  cliffs  from  Greene  County,  Pennsylvania, 
clear  across  West  Virginia  to  the  Big  Kanawha  River  at  Winfield. 

This  stratum  is  the  only  one  in  the  series  that  is  generally  con- 
glomeratic or  contains  quartz  pebbles  larger  than  coarse  sand  grains. 
On  account  of  this  peculiarity  the  rock  in  question  becomes  a very  im- 
portant guide  to  the  geologist  in  the  interior  of  West  Virginia,  where 
so  many  of  the  Dunkard  Creek  coals  and  limestones  have  disappeared, 
for  it  retains  its  pebbly  character  over  a very  wide  area.  When  at  its 
greatest  development  the  thickness  of  this  stratum  approaches  75  and 
even  100  feet.  It  is  usually  a grayish  white  rock,  with  a yellowish 
cast  on  freshly  broken  surfaces,  and  its  weathered  bowlders  are  usually 
covered  with  ridges  and  streaks  of  harder  iron -bearing  sand.  The  rock 
splits  readily  and  frequently  furnishes  excellent  building  stone,  the 
piers  of  the  Baltimore  and  Ohio  Railroad  bridges  across  the  Monongahela 
River  near  Fairmont  having  been  constructed  of  it. 

Along  the  western  border  of  the  outcrop  of  this  rock  it  dwindles 
down  and  changes  its  character  entirely,  being  frequently  represented 
in  Washington  County,  Pennsylvania;  Marshall  and  Ohio  Counties, 
West  Virginia ; Belmont  and  Monroe  Counties,  of  Ohio,  by  sandy  shales 
and  flaggy  sandstones,  and  occasionally  even  a stratum  of  limestone 
may  be  found  at  this  horizon. 

In  passing  down  the  Ohio  River  below  Marshall  County  the  horizon 
of  this  sandstone  passes  below  water  level,  but  when  it  reappears  near 
Saint  Mary’s,  in  P leasants  County,  the  rock  has  regained  its  massive- 
ness, and  is  a coarse  pebbly  sandstone  50  feet  thick,  and  from  this 
point  on  down  the  Ohio  River,  whenever  above  the  level  of  the  same, 
it  is  always  a massive  sandstone.  From  Blennerhasset  Island,  below 
Parkersburg,  this  rock  is  almost  constantly  visible  either  in  the  bed 
or  bluffs  of  the  Ohio  on  down  to  25  miles  below  the  mouth  of  the 
Great  Kanawha.  It  is  the  emergence  of  this  stratum  from  the  bed  of 
the  stream  which  makes  Letart  Falls  in  the  Ohio  River.  It  is  this  rock 
which  forms  the  great  cliffs  in  the  top  of  the  hills  at  Red  Rock,  in  Put- 


WHITE.] 


AGE  OP  THE  DUNKARD  CREEK  SERIES. 


41 


narn  County,  on  the  Great  Kanawha,  and  the  same  may  be  seen  as  a 
bed  of  pebbly  sandstone  at  many  points  in  Ritchie,  one  at  the  famous 
Grahamite  mine  being  especially  noteworthy,  for  it  is  the  great  sand- 
rock  through  which  the  celebrated  fissure  extends  at  the  base  of  the 
hills,  and  it  is  there  75  feet  thick. 

Through  Ritchie,  Gilmer,  and  Calhoun  Counties  a bed  of  brecciated 
limestone  occurs  at  the  base  of  this  stratum  and  incorporated  with  it, 
which  is  quite  persistent  and  seems  to  replace  the  usual  underlying 
Wavnesburg  coal,  which  is  there  absent. 

THE  CASSVILLE  PLANT  SHALE. 

The  Waynesburg  sandstone  often  rests  directly  on  the  underlying 
Waynesburg  coal,  but  more  frequently  a bed  of  dark  gray  shale,  5 to 
15  feet  thick,  intervenes.  This  shale  is  always  prolific  in  fossil  plants  and 
is  especially  so  in  the  vicinity  of  Cassville,  Monongalia  County,  West 
Virginia.  It  is  from  this  locality  and  horizon  that  so  many  of  the  fos- 
sil plants  were  obtained  which  are  described  in  the  Second  Geological 
Survey,  Pennsylvania,  Report  PP,  by  Fontaine  and  White,  and  it  is 
from  the  same  shale  that  so  many  plants  of  Permian  and  even  Triassic 
types  have  been  procured,  Tseniopteris,  Saportma,  Baiera,  and  Pa- 
chypteris  being  among  the  number.  No  systematic  search  has  ever 
been  made  at  any  other  locality,  and  hence  it  is  entirely  probable  that 
the  list  of  fossil  plants  could  be  largely  increased  were  this  bed  thor- 
oughly explored  in  other  regions.  Other  promising  localities  of  the 
Cassville  shale  which  have  been  slightly  explored  are  CarmichaePs, 
Greene  County,  Pennsylvania;  Georgetown,  Monongalia  County ; and 
West  Union,  Doddridge  County.  In  connection  with  these  roof  shales, 
and  sometimes  interstratified  with  the  top  members  of  the  underlying 
coal,  there  occur  at  Cassville  numerous  remains  of  insects,  the  princi- 
pal ones  being  fossil  cockroaches,  of  which  Gerablattina  seems  to  be 
the  principal  genus. 

THE  AGE  OF  THE  DUNKARD  CREEK  BEDS. 

The  fauna  of  these  rocks  has  never  been  systematically  studied  and 
its  relationships  determined.  What  desultory  work  has  been  done  in 
this  line  goes  to  show  that  the  animal  forms  consist  principally  of  mi- 
nute shells  of  crustaceans,  fish  remains,  and  insects,  many  of  which  are 
probably  undescribed.  No  Brachiopods  have  ever  been  seen  in  these 
rocks,  and  hence  one  important  line  of  evidence  which  might  help  to 
determine  their  relative  age  is  wanting.  Some  geologists  have  been 
inclined  to  regard  them  as  belonging  in  the  Carboniferous  proper  be- 
cause of  the  absence  of  the  Permian  reptilian  fauna,  and  other  types 
common  elsewhere,  but  as  the  deposits  are  mainly  of  fresh  water  origin, 
the  absence  of  such  types  is  to  be  expected.  Hence  until  the  minute 
fauna  occurring  in  these  limestones  and  black  slates  shall  have  been 
carefully  studied,  the  geologist  must  rely  on  the  evidence  of  fossil  plants. 


42  THE  NORTHERN  BITUMINOUS  COAL  FIELD  [bull.  65. 

These  have  been  studied  by  Prof.  Wm.  M.  Fontaine  and  the  writer, 
the  results  being  published  in  Report  TP,  Second  Geological  Survey, 
Pennsylvania.  The  conclusions  there  given  show  that  the  flora  is 
closely  ana  unmistakably  allied  to  the  Permian  of  Europe,  since  it  con- 
tains so  many  types  that  are  peculiar  to  those  rocks  or  even  related  to 
Mesozoic  forms.  The  facts  and  conclusions  set  forth  are  sufficient  to 
convince  Prof.  Archibald  Geikie  that  these  rocks  are  of  the  same  age 
as  the  reptiliferous  beds  at  Autun. 

The  conclusion  that  these  rocks  are  of  Permian  age  has  not  been  ac- 
cepted by  all  American  geologists,  though  none  have  given  any  reasons 
for  discrediting  the  evidence  of  the  fossil  plants  on  which  it  is  based, 
and  until  it  is  contradicted  by  the  animal  remains  or  otherwise  shown 
to  be  erroneous,  no  other  hypothesis  is  tenable  in  view  of  the  evidence 
at  hand.  The  list  of  plants  from  which  the  Permian  age  of  these  Dunk- 
ard  beds  is  inferred,  together  with  the  general  discussion  of  the  same, 
is  given  m Chapter  III,  pages  105,  120,  Report  PP,  Second  Geological 
Survey,  Pennsylvania. 

The  recent  discovery  of  an  undoubted  Permian  invertebrate  fauna  in 
Texas  by  Prof.  C.  A.  White  and  Mr.  Cummins  (American  Naturalist, 
February,  1889),  confirms  the  conclusions  of  Profs.  Cope  and  Marcou 
with  reference  to  the  existence  of  a great  Permian  series  of  rocks  in 
this  country,  and  hence  there  is  no  longer  any  reason  for  doubting  that 
America  contains  deposits  which  are  equivalent  in  part  at  least  to  the 
Permian  of  Europe.  The  Texas  deposits,  as  described  by  Prof.  White 
in  the  article  referred  to,  are  so  exactly  similar  lithologically  to  these 
uppermost  beds  of  the  Appalachian  region,  that  the  description  of  the 
one  might  well  answer  for  that  of  the  other,  and  there  can  be  very  little 
doubt  that  the  two  series  are  equivalent.  Singularly  enough  the  beds 
have  practically  the  same  thickness,  1,000  feet  in  Texas,  and  1,100  in 
West  Virginia  and  southwest  Pennsylvania. 


CHAPTER  III. 


THE  UPPER  COAL  MEASURES,  OR  MONONGAHELA  RIVER  SERIES. 

THICKNESS,  CHARACTER,  AND  EXTENT. 

This  series  of  rocks  begins  at  base  with  the  Pittsburgh  coal  and 
extends  up  to  the  Cassville  shale.  The  thickness  varies  between  200 
feet  along  the  northwestern  outcrop  in  Ohio  and  380  feet  in  the  Monon- 
gahela  River  region,  but  in  the  center  of  the  Appalachian  trough  a 
boring  at  Browntown,  Harrison  County,  West  Virginia,  carefully  meas- 
ured with  steel  line,  reveals  a thickness  of  413  feet  from  the  top  of  the 
Waynesburg  coal  to  the  bottom  of  the  Pittsburgh  bed. 

Within  the  interval  there  belong  six  distinct  coal  beds,  though  only 
four  of  these  are  workable  over  any  considerable  area.  These  coals 
have  their  greatest  development  along  the  waters  of  the  Monongahela 
River,  and  hence  the  series  was  long  ago  named  after  that  river  by 
Prof.  H.  D.  Rogers. 

The  character  of  the  rocks  interstratified  with  the  coal  beds  changes 
greatly  in  passing  from  the  Monongahela  River  southward  to  the  Great 
Kanawha.  At  the  northern  end  of  the  basin  in  Marion,  Monongalia, 
Greene,  Washington,  Fayette,  and  Westmoreland  Counties,  limestone 
forms  about  one-half  of  the  rock  material,  and  the  same  is  true  on  the 

N 

western  side  in  Brooke,  Ohio,  Marshall,  and  Belmont  Counties.  Red 
shale  is  unknown  in  the  series  at  the  north,  but  in  passing  southward 
from  Harrison  and  Lewis  Counties  the  limestones  practically  disap- 
pear, and  with  them  all  of  the  coals  except  the  Pittsburgh.  With 
their  disappearance  red  shales  come  in  and  apparently  replace  the 
limestones,  so  that  on  the  Great  Kanawha  nearly  one-fourth  of  the 
rock  material  in  this  series  is  red  shale,  while  the  thickness  is  reduced 
to  270  feet.  Along  with  this  change  in  the  character  of  the  rocks 
there  occurs  a great  change  in  the  topography  made  by  these  beds,  for 
at  the  north,  where  limestone  is  abundant,  sandstones  are  few  and 
shaly,  so  that  a gentle,  rolling  topography  results,  with  a very  rich  soil 
and  one  of  the  finest  grazing  and  farming  regions  in  the  country,  while 
to  the  southwest,  after  the  limestones  have  disappeared  the  sand- 
stones thicken  up  and  become  more  massive,  thus  giving  rugged  and 
precipitous  slopes  with  narrow  valleys. 


43 


44 


THE  NORTHERN  BITUMINOUS  COAL  FIELD. 


[BULL.  65. 


The  character  of  the  Upper  Coal  Measure  rocks  in  the  several  portions 
of  the  area  they  occupy  is  shown  by  the  several  sections  which  follow. 
Section  in  Fayette  and  Westmoreland  Counties , Pennsylvania. — Prof. 

Stevenson,  who  has  done  so  much  to  elaborate  the 
detailed  structure  of  this  series,  gives  the  following 
(Fig.  11),  in  Second  Geological  Survey,  Pennsylvania, 
Eeport  KK,  page  31,  as  the  general  section  of  these 
beds  in  Fayette  and  Westmoreland  Counties : 


Fayette  and  Westmoreland  Counties,  Pennsylvania. 


[See  map,  K n.] 


\t£ 


1.  Coal,  Waynesburg 

2.  Sandy  shales  or  sandstone 

3.  Coal.  Little  Waynesburg  .. 

4.  Limestone,  Waynesburg... 

5.  Shale  and  shaly  sandstone 

6.  Coal,  TJniontown 

7.  Limestone,  TJniontown 

8.  Sandstone 

9.  Limestone,  “ Great” 

10.  Coal,  Sewiekley 

11  Sandstone 

12.  Limestone,  Sewiekley 

13.  Shale  or  shaly  sandstone... 

14.  Coal,  Redstone 

15.  Limestone,  Kedstone 

16.  Sandstone  or  shale 

17.  Coal,  Pittsburgh 


Ft. 

20 

2 

20 

50 

12 

30 

80 

30 

25 

20 

10 

40 


Ft. 


92 


122 


75' 


Total . 


367 


Section  at  Broicnsville , Pennsylvania . — At  Browns- 
ville, Fayette  County,  Pennsylvania, 

Prof.  Stevenson  finds  the  following 
structure,  (Fig.  12),  for  this  series,  as 
given  in  KK,  page  233  : 


Fig.  11.— Section  in 
Fayette  and  West- 
moreland Coun- 
ties, Pa. 

Brownsville,  Fayette  County,  Pennsylvania. 

[See  map,  K m.]  Ft.  in. 

1.  Coal,  Waynesburg,  blossom 

2.  Shales,  sandy 45 

3.  Coal,  Little  Waynesburg,  blossom 0 

4.  Limestone.  Waynesburg 4 

5.  Shales  and  shaly  sandstone 55 

6.  Coal,  Uniontown,  blossom 

7.  Limestone,  coarse,  yellow 1 

8.  Clay 3 

9.  Shale  and  sandstone 16 

10.  Limestone 2 

11.  Concealed 17 

12.  Sandstone 3 

13.  Limestone  with  shales 42 

14.  Concealed 16 

15.  Limestone 6 

16.  Concealed 7 

17.  Clay  shale 8 

18.  Sewiekley  coal  horizon 

19.  Sandy  shale  and  flaggy  sandstone 30 

20.  Limestone 30 

21.  Shale 35 

22.  Coal,  Kedstone 

23.  Shale,  sandy 

(Coal.... O'  8" 

24.  Coal,  Pittsburgh < Clay O'  10" 

(Coal  ..7'  6" 

Total 


354 


Fig.  12.— Section  at 
Brownsville,  Pa. 


GEOLOGICAL  SURVEY 


UPPER  COAL  MEASURES  CAPPED  WITH  PERMO-CARBONIFEROUS  BEDS,  WHEELING,  WEST  VIRGINIA. 


* THE  LIBRARY 
OF  THE 

UNIVERSITY  OF  ILLINOIS 


WHITE.] 


SECTION  AT  RICE’S  LANDING,  PA. 


45 


Section  at  West  Brownsville , Pennsylvania. — On  the  opposite  side  of 
the  Monongaliela  Biver,  in  descending  from  Kreb’s  Knob  to  West 
Brownsville,  in  Washington  County,  the  writer  meas- 
ured the  several  members  of  this  series  with  the  fol- 
lowing results  (Fig.  13) : 


40' 


96'6" 


West  Broivnsville,  Washington  County , Pennsylvania . 

fSee  map,  K m.] 


( Coal . 

Coal,  Waynesburg ' Clay 0' 


its' 


Ft.  in. 

.0'  10 

, 3 

( Coal 2'  6 

Shales  and  sandstone 45 

Bitumenous  shale.  Little  Waynesburg  Coal 1 

Limestone,  Waynesburg.-. 10 

Sandstone,  shaly 40 

Coal,  Uniontown 

Limestone,  Uniontown 12 

Shale  and  sandstone 28 

Limestone,  with  thin  shales  .... 88 

Coal,  Sewieklev,  blossom  

Sandstone,  shaly 32 

Limestone 30 

Shales 20 

Coal,  Redstone 

Sandstone  and  shales 

fCoaL.O'  3"] 

Coal,  Pittsburgh,  roof <j  ‘ J',  | 2 

(ciay.-l'  0"J 

Coal,  Pittsburgh,  main  bench 7 


6 I 


Ft.  in. 

3 7 


96  6 


3 

128 


82 


Total. 


9 6 


308  7 


Fig.  13.— Section  at 
West  Brownsville, 
Pa. 


Section  at  Bice’s  Landing , Pennsyl- 
vania.— In  the  steep  hillside,  one  mile 
below  Bice’s  Landing,  Greene  County, 
Pennsylvania,  the  series  exhibits  the 
following  structure  (Fig.  14) : 


Rice' 8 Landing,  Greene  County,  Pennsylvania. 

[See  map,  K m.] 


Ft.  in.  Ft.  in. 


fCoal. 

...V 

0" 

1 Clay. 

...0' 

5" 

1.  Waynesburg  coal...  < Coal. 

...r 

3" 

1 Clay. 

...r 

2" 

[Coal. 

...2' 

6" 

2.  Shales 40 

3.  Limestone,  Waynesbnrg 6 

4.  Shales  and  sandstone 45 

5.  Coal,  Uniontown 

6.  Limestone,  Uniontown 6 

7.  Shales  and  sandstone 38 

8.  Limestone,  “ Great  ” 82 

9.  Coal,  Sewickley , 

10.  Sandstone 40 

11.  Limestone 25 

12.  Sandy  shale 30 

13.  Slate,  bituminous  (Redstone  coal) 

14.  Sandstone,  Pittsburgh,  flaggy 15 

15.  Sandstone,  Pittsburgh,  massive 30 

( C Coaly  shale 

[ Roof.  < Coal 

16.  Coal,  Pittsburgh.. . ^ f. Clay 

{ Main  bench 7' 

Total 


6 4 
91 

1 6 
126 
1 9 
95 
1 6 
45 

10 

378  1 


fjgiill 

6V 

ifUii 

4& 

a* 

=•  =r— — 

6 

4S' 

i'6"J 

6' 

3&' 

, ■ ■ • ; • ; g 

KBS 

82' 

if ; 

;S 

4 O' 

25’ 

■ 

3 O’ 

l’6\ 

15’ 

30 

SSlISSffi 

io’ 

Flo.  14.— Section  at 
Rice’s  Landing,  Pa. 


46  THE  NORTHERN  BITUMINOUS  COAL  FIELD.  [bull.  65. 

Section  on  Robinsorts  Run . West  Virginia. — The  Upper  Goal  Measure 
beds  attain  a very  fine  development  in  Monongalia  County,  West 
Virginia,  just  south  from  the  Greene  County  line,  and  there,  on  Eobin- 
son’s  Eun,  2 miles  west  from  the  Monongahela  Eivefc,  the  following 
succession  (Fig.  15)  is  exposed : 


33? 

ft 

O* 

f 

40’ 

ijjgjgg 

3" 

a' 

5 

7: : ■ : 

* 

sf 

1 

i 

f 

10' 

SIM* 

* 

|Mll 

is' 

A 

K>' 

20' 

IHHHfldl 

9. 

a* 

Fig.  15. — Section  on 
Bobinson’s  Kun, 
W.  Va. 


Bobinson’s  Bun,  Monongalia  County , West  Virginia. 

[See  map,  L m.] 

Ft.  in. 


f Coal... 2'  6” 

1.  Coal,  Waynesburg  . . < Shale.  .1'  6" 

( Coal  . .4'  0" 

2.  Sandy  shales  with  iron  ore  below  middle 35 

3.  Limestone,  Waynesburg 8 

4.  Shales 10 

5.  Limestone *. 1 

6.  Sandstone,  flaggy 40 

7.  Black  slate  (Uniontown  coal) 5 

8.  Limestone,  Uniontown 10 

9.  Sandstone  and  shales 35 

10.  Limestone 6 

11.  Shales 10 

12.  Sandstone,  flaggy 30 

13.  Limestone,  cement  beds 20 

14.  Sandstone,' "Sewickley  35 

15.  Coal,  Sewickley 

16.  Shales 10 

17.  Limestone 10 

18.  Shales 12 

19.  Limestone 18  ‘ 

20.  Shales 15 

21.  Coal,  Bedstone 

22.  Limestone,  Bedstone 10 

23.  Shales  and  slates 20 


24.  Coal,  Pittsburgh. 


( Boof  coals  - .3'  ) 

\ Clay l'[ 

(Coal 8'  ) 


Ft.  in 

8 


94 


151 


65 


30 


12 


Total 


Here,  as  will  be  seen  from  the  above  section,  the  Eedstone  coal, 
which  belongs  between  the  Pittsburgh  and  Sewickley  beds,  has  thick- 
ened up  into  merchantable  condition.  This  coal  contains  a little  more 
sulphur  than  either  the  Pittsburgh  below  or  the  Sewickley  above,  but 
it  makes  a very  fair  fuel  for  domestic  and  steam  producing  purposes. 
It  is  softer  than  either  of  the  other  two  and  would  coke  well. 

The  Eedstone,  Pittsburgh,  and  Sewickley  beds  of  this  section  foot 
up  a total  thickness  of  21 J feet,  including  partings,  and  about  17  feet 
of  this  is  merchantable  coal. 


WHITE.] 


SECTION  ON  SCOTT’S  RUN,  WEST  VIRGINIA.  47 

Section  on  Scotfs  Run , West  Virginia. — A short  distance  south  from 
Robinson’s  Run,  we  get  another  fine  exposure  of  the  Upper  Coal  Meas- 
ure beds  along  the  waters  of  Scott’s  Run,  between  Cassville  and  the 
mouth  of  the  stream,  as  follows  (Fig.  16) : 

Scotfs  Bun,  Monongalia  County,  West  Virginia. 


[See  map,  M m.] 


1.  Coal, Way nesburg. 


2.  Black  slate. 


os* 


Fig.  16. — Section  on 
Scott’s  Run,  W.Va. 


f Coal 2'  0"1 

f Shale,  fossiliferous..l'  0"  | 

{ Coal 1'  4"  > 

| Shale,  gray V 6"  | 

[Coal 1 5'  0” J 


3.  Sandy  shales,  with  iron  ore 

4.  Limestone,  W aynesburg 

5.  Sandy  shales,  with  limestone  layers 

6.  Sandstone,  massive 

7.  Limestone  and  shales 

8.  Black  slate,  representing  Uniontown  coal 

9.  Limestones,  interstratified  with  thin  shales,  cement 

beds  near  base 

10.  Sandstone,  Sewickley 

11 . Coal,  Sewickley 

12.  Shales 

13.  Sandstone 

14.  Limestone - 

15.  Shales,  greenish  gray 

16.  Concealed 

17.  Limestone,  steel  gray 

18.  Concealed  

19.  Coal,  Redstone 

20.  Li  mestone,  Redstone - 

21.  Shale  and  fire  clay 

22.  Slate,  black 

( Coal.  0'  3"  I 

23.  Coal,  Pittsburgh,  roof i CoS!.'?  0"  f 

L Clay! . V 0"  J 

( Coal.. 3'  6" 

Slate  .0' 

| Coal.. O'  8" 

| Slate. O'  1" 

24.  Coal,  Pittsburgh,  main  bench  ..  ^ Coal.  .1'  6"  

[ Slate. 0' 

Coal.. O'  6" 

I Slate. 0'  | 

l Coal.. 3'  3" J 

Total 


Ft.  in. 


Ft.  in. 
10  10 


105 

40 

5 

10 

5 

8 

15 

7 

15 

18 

5 

5 


2 

145 

5 

65 

4 

28 


13  10£ 


9 7i 


372  8& 


The  same  Redstone  coal  makes  its  appearance  in  this  section  ; in  fact 
it  underlies  all  of  the  region  intervening  between  Scott’s  and  Robin- 
son’s Runs,  thinning  out  southward  as  well  as  northward.  It  underlies 
an  area  of  probably  5,000  acres  where  it  is  of  workable  thickness.  In 
the  oil-well  borings  on  Doll’s  Run,  and  as  far  west  as  Mannington  and 
Fairview,  this  bed  is  still  present,  though  apparently  not  of  workable 
thickness. 


48 


THE  NORTHERN  BITUMINOUS  COAL  FIELD, 


[BULL.  65. 


Section  on  Buffalo  Creek , West  Virginia. — Along  Buffalo  Creek,  in 
the  vicinity  of  Fairmont,  Marion  County,  West  Virginia,  the  Upper 
Coal  Measures  exhibit  the  following  succession  (Fig.  17): 

Buffalo  Creek,  Marion  County , West  Virginia. 


[See  map,  M 1.] 

f Coal...  O'  6"  1 
i Shale.. O'  1"  | 

1.  Coal,  Waynesburg •(  Coal. . 1'  0"  V ... 

I Shale..  1'  4" 

1 Coal.  ..3'  0'' J 

2.  Shales 

3.  Sandstone,  massive 

4.  Shale 

5.  Limestone,  Waynesburg 

6.  Shales 

7.  Limestone 


Fig.  17. — Section  on 
Buffalo  Creek,  W.  Va. 


8.  Shales  r 

9.  Sandstone 

10.  Shales 

11.  Coal,  Uniontown 

12.  Fire  clay 

13.  Sandstone 

14.  Shales  and  black  slate 

15.  Limestone 

16.  Fire  clay 

17.  Shales  with  limestone 

18.  Sandstone 

19.  Blue  shale 

20.  Limestdfre 

21.  Shales  and  concealed 

22.  Limestone  interstratified  with  thin  shales 

23.  Shales 

fCoal 5'  0"1 

I Clay O'  4'  j 

24.  Coal,  Sewickley Coal 0'  4"  } .. 

I Slate,  dark  .0'  3"  J 

[Coal O'  5"  j 

25.  Shales 

26.  Limestone,  buff 

27.  Sandstone,  gray,  massive 

28.  Limestone,  gray 

29.  Concealed  and  shales 

30.  Impure  clay 

31.  Limestone  and  shales 

32.  Sandstone,  Pittsburgh 

33.  Shales 

f Coal,  bony.  0'  10"  1 

I Bone O'  l\" 

I Coal 2'  3" 

34.  Coal,  Pittsburgh. . . Slate 0'  i"  } 

I Coal 0'  5" 

[Slate 0'  i"| 

[Coal  3'  5£" J 

Total 


!.  in.  Ft.  in. 

5 11 


20 

30 

3 

1 6 
18 

1 6 
12 
10 
5 

4 
1 

5 
3 
5 
5 
2 


> 101 


2 6 


149 


1 

25 

85 

5 


J 


6 4 


3 6 

4 
18 

5 

15 

5 

20 

25 

5 


100  6 

I 


7 1* 


372  4$ 


The  portion  of  this  section  from  the  Sewickley  coal  down  to  the  base 
of  the  series  was  measured  at  the  Montana  mines,  2J  miles  below  the 
mouth  of  Buffalo  Creek. 

The  Redstone  coal  is  entirely  absent  here,  its  horizon  being  occupied 
by  the  5 feet  of  impure  fire  clay,  50  feet  above  the  Pittsburgh  bed. 

Section  at  Clarksburg , West  Virginia. — In  passing  from  Marion  County 
southward  towards  Clarksburg,  in  Harrison  County,  a great  change 
takes  place  in  the  character  of  the  sediments  of  the  Upper  Coal  Meas- 


WHITE.] 


SECTION  AT  WHEELING,  W.  VA. 


49 


ures.  The  limestones,  so  prominent  in  Greene,  Monongalia,  and 
Marion,  dwindle  down  to  insignificant  proportions,  as  shown  by  the  fol- 
lowing section  (Fig.  18),  made  at  Clarksburg  by  Mr.  Jno.  L.  Johnston, 
civil  engineer : 


Clarksburg,  Harrison  County,  West  Virginia. 


Fig.  18.— Section  at 
Clarksburg,  W.  Va. 


[See  map,  Ok.] 

1.  Waynesburg  coal,  absent  or  not  seen 

2.  Concealed  and  yellow  sandy  shales 65 

3.  Sandstone 25 

4.  Concealed,  with  some  limestone - 80 

5.  Sandstone 20 

6.  Concealed 5 

7.  Sandstone 15 

8.  Sandy  shales 6 

9.  Sandstone,  Sewickley 25 

10.  Shales 10 

11.  Coal,  Sewickley 

12.  Limestone {lood":#  6"}“" 9 

13.  Concealed 3 

14.  Shales,  sandy 14 

15.  Shale,  with  iron  nodules 1 

16.  Shales,  sandy 4 

17.  "Sandstone 1 

18.  Concealed 8 

19.  Coal,  Redstone,  slaty 

20.  Shale,  dark,  bituminous 5 

21.  Limestone,  Kedstone 6 

22.  Shale,  greenish 13 

23.  Slate,  bituminous , 1 

( Coal 3 5' 

24.  Coal,  Pittsburgh  . { Bone  ...  O'  1 


Ft.  in. 


I Coal 5'  0‘ 


Ft.  in. 
0 


> 251 


40 


Total 


328  6 


Section  at  Cliapline  Hill , Wheeling , West  Virginia . — Between  the  Monon- 


gahela  and  Ohio  Rivers  a considerable  change  takes  place 
in  the  character  of  the  Upper  Coal  Measure  beds,  and 
also  in  the  thickness  of  the  several  members,  as  will  be 
seen  by  the  following  section  (Fig.  19)  from  Chapline 
Hill,  Wheeling,  West  Virginia: 

Chapline  Hill,  Wheeling,  West  Virginia. 

Ft.  in. 

1 


[See  map,  K j.] 

1.  Coal,  Waynesburg ' 

2.  Concealed 5 

3.  Flaggy  sandstone,  filled  with  plant  fragments 4 

4.  Concealed 4 

5.  Limestone,  shales  and  concealed 60 

6.  Sandstone,  massive,  gray 5 

7.  Limestone  and  concealed 20 

8.  Green  shale 5 

9.  Limestone,  interstratified  with  shales 55 

C Coal . . 1 

10.  Coal,  Sewickley. < Sandy  shales  with  plants 12 

( Cos  ’ 


Ft.  in. 
2 


158 


11.  Sbales 8 

12.  Sandstone,  rather  massive,  micaceous,  current-bedded 20 

13.  Limestone,  impure,  flaggy,  filled  with  fossil  ferns 1 

14.  Coal,  Redstone 

15.  Limestone,  mostly  bnffish  and  impuro. 

C Coal,  roof 2' ' 

16.  Pittsburgh  coal < Shale 

( Coai,  main  bench. 


0 ) 
! 


1 


13  8 


29 


0 10 
55 


60' 


15tf 


20' 


Total 

Bull.  65- 


267 


Fig.  19.— Section  at 
— Chap  lino  Hill, 
6 Wheeling,  W.Va. 


50 


THE  NORTHERN  BITUMINOUS  COAL  FIELD. 


[BULL.  65. 


Here  the  Waynesburg  coal  has  dwindled  to  an  unimportant  bed, 
and  the  Sewickley  has  split  into  two  portions  separated  by  12  feet  of 
shales,  while  the  whole  column  has  lost  more  than  100  feet  of  thick- 
ness compared  with  the  Monongahela  River  region. 

Section  near  Bellaire , Ohio. — At  Bellaire,  Ohio,  4 miles  below  Wheel- 
ing, the  following  carefully  leveled  section  (Fig.  20)  was  made  by  Prof. 
0.  N.  Brown,  of  the  present  Ohio  Geological  Survey.  It  exhibits  some 
interesting  changes  as  compared  with  the  Wheeling  section : 


Near  Bellaire , Belmont  County,  Ohio. 


[See  map,  K i.] 


Ft.  in.  Ft.  in. 


1.  Coal,  Waynesburg 

2.  Shale,  sandy 

3.  Shale 

4.  Limestone 

5.  Concealed 

6.  Coal,  blossom,  Little  Waynesburg 

7.  Concealed 

8.  Coal,  blossom,  Uuiontown 

9.  Shale 

10.  Sandstone 

11.  Shale,  argillaceous 

12.  Concealed...... : 

13.  Shale  

14.  Sandstone - 

15.  Shale 

16.  Concealed 

17.  Calcareous  shale,  -with  thin  limestones 

f Coal 4'  0"1 

j Shales,  sandy 13'  10"  ! 

18.  Coal,  Sewickley Coal O'  8"  } ... 

| Shale,  argillaceous  6'  0"  } 

l Coal -. 3'  0"  J 

19.  Shale,  argillaceous 

20.  Limestone,  thin  clay  in  center 

21.  Limestone,  magnesian,  cement  rock 

22.  Clay 1 

23.  Limestone 

24.  Concealed 

25.  Coal,  Redstone,  blossom 

26.  Concealed 

27.  Shale - 

28.  Coal,  Pittsburgh 

Pig.  20. — Section  near 

Bellaire,  Ohio.  Total 


6 

12 

3 

5 

14 

4 

6 

20 

32 
2 
3 
3 

33 

24  6 


2 

8 

5 

1 

11 

11 

17 

1 


<1 


2 


40 


J 

1 


127  6 


27  6 


38 

2 

18 

7 

263 


The  interval  between  the  two  members  of  the  Sewickley  coal  has 
here  increased  to  20  feet,  and  the  upper  one  seems  to  keep  permanently 
above  the  lower  one  from  here  southwest  ward  through  Ohio,  becoming 
the  Cumberland  and  Meigs  Creek  bed  of  the  Ohio  geologists. 

Both  the  Little  Waynesburg  and  Uniontown  coals  are  represented 
in  this  section,  but  neither  one  was  observed  at  Wheeling. 

It  is  worthy  of  note  that  there  is  a difference  of  only  4 feet  in  the 
total  thickness  of  the  Upper  Coal  Measures  as  given  by  Prof.  Brown’s 
section  at  Bellaire  and  mine  at  Wheeling,  four  miles  above. 


BULLETIN  NO.  65  PL. 


UPPER  COAL  MEASURES  AND  PERMO-CARBONIFEROUS,  POWHATAN,  OHIO. 


THE  LIBRARY 
OF  THE 

UNIVERSITY  OF  ILLINOIS 


WHITE.  1 


SECTION  ON  PIPE  CREEK,  OHIO. 


51 


Section  at  Moundsville , West  Virginia.—* Near  the  mouth  of  Grave 
Creek,  one  mile  below  Moundsville,  West  Virginia,  and  7 miles  below 
Bellaire,  these  measures  exhibit  the  following  succession  by  combining 
the  surface  exposures  with  the  record  of  an  oil  boring  (Fig.  21) : 


zo- 


Fig.  21. — Section  at 
Moundsville,  W.  Va. 


Moundsville , Marshall  County , West  Virginia. 

[See  map,  K i.] 

Ft.  in. 

l Coal,  impure . . 0 ' 6"  ) 

1.  Coal,  Waynesburg < Shale V 0"  > 

( Coal V 6") 

2.  Shale,  soft,  gray 5 

3.  Sandstone,  massive,  gray,  micaceous 20 

4.  Concealed,  with  limestone  layers  at  base  2 feet  thick 20 

5.  Flaggy  sandstone  and  sandy  shales 20 

6.  Concealed 10 

7.  Limestone 1 

8.  Concealed 14 

9.  Limestone,  gray 22 

10.  Concealed  to  mouth  of  oil  and  gas  well  at  30  feet  above 

low- water  mark  in  Ohio  Fiver 28 

11.  Conductor  hole  of  oil-well  record 18 

12.  Limestone,  light  gray 40 

13.  Slate • 15 

14.  Black  rock,  shales 10 

15.  Coal,  Bedstone : 

16.  Fire  clay 7 

17.  Hard  slate  4 

18.  Gray  limestone 20 

19.  Bastard  limestone 10 

20.  Coal,  Pittsburgh 


Ft  in. 
3 


223 


Total 


274  6 


Section  on  Pipe  Greek , Ohio. — Pipe  Creek  puts  into  the  Ohio  Eiver 
3 miles  below  the  mouth  of  Grave  Creek,  and  there,  on  the  Belmont 
County  side  of  the  river,  the  Pittsburgh  coal  is  at  low-water  level.  The 
following  structure  (Fig.  22)  is  found  in  the  steep  hills  which  border 
the  mouth  of  Pipe  Creek : 


Pijje  Creek , Belmont  County , Ohio. 

[See  map,  K i.] 


1.  Coal,  Waynesburg,  slaty  at  top 

2.  Concealed,  limestone  and  shales 

3.  Bituminous  slate,  Uniontown  coal 

4.  Limestone,  Uniontown 

5.  Concealed,  with  much  limestone 100 


Coal,  and  coaly  shale. 

2' 

0" 

Sandstone  

!l2' 

0" 

Coal 

. O' 

4" 

Shale 

. 1' 

0" 

Coal 

4" 

Shale,  sandy  

. 5' 

0" 

Coal,  slaty  

. 1' 

8" 

Shale 

. O' 

4" 

Coal 

. 1' 

0" 

Black  slate 

. 0' 

4" 

7.  Limestone,  Sewickley,  and. shales 

8.  Bituminous  shale,  (Redstone  coal)  ... 

9.  Limestone,  (Redstone)and  concealed. 

10.  Coal,  Pittsburgh 


Total. 


Feet. 

Feet. 

4 

55 

1 

..  10  i 

i 110 

24 

22 

1 

25 

6 

248 

Fig.  22.— Section  in 
Bel  m out  County, 
Ohio. 


52 


[BULL.  65 


THE  NORTHERN  BITUMINOUS  COAL  FIELD. 

Below  this  last  locality  no  measurement  of  the  Upper  Coal  Measure 
series  is  possible  for  a long  distance,  because  most  of  the  members  are 
below  water  level.  They  are  all  brought  to  the  surface,  however,  by 
the  Volcano  anticline,  which  crosses  the  Ohio  River  from  Pleasants 
County,  West  Virginia,  into  Washington  County,  Ohio. 

Section  in  Washington  County , Ohio . — Mr.  F.  W.  Minshall,  of  Marietta, 
Ohio,  has  made  a very  careful  study  of  these  measures  in  Washington 
County,  Ohio,  and  has  prepared  the  followiug  section  (Fig.  23)  as  rep- 
resenting their  usual  structure  there : 

Washington  County , Ohio. 


[See  map,  M g.J 


Fig.  23. — Section  in 
Washington  County, 
Ohio. 


1.  Coal,  Waynesburg  (Macksburg) 

2.  Shale  

3.  Sandstone 

4.  Shale 

5.  Limestone 

6.  Shaly  sandstone 

7.  Limestone  and  shale 

8.  Coal,  Sewickley  (Meigs  Creek) . . 

9.  Shales  and  limestone 

10.  Shales . 

11.  Sandstone  

12.  Shales 

13.  Coal,  Pittsburgh,  thin .. 

Total 


Ft.  in.  Ft.  in. 


14 

11 

18 

6 

18 

29 

25 

40 

19 

4 


4 


> 96 


2 6 


190  6 


The  thickness  here  given  is  50  to  60  feet  less  for  the  entire  series  than 
that  usually  found  in  any  other  portion  of  the  Appala- 
chian field. 

Section  at  Burning  Springs , West  Virginia. — In  the  vi- 
cinity of  Burning  Springs,  Wirt  County,  West  Virginia, 
these  rocks  are  brought  above  the  surface  by  the  same 
anticline,  and  there  Mr.  Minshall  reports  the  following 
structure  (Fig.  24) : 


Burning  Springs,  Wirt  County,  West  Virginia. 


' Z07' 


[See  map,  P g.] 

1.  Coal,  Waynesburg 

2.  Concealed  and  shales 

3.  Sandstone,  Pittsburgh 

4.  Shales  

5.  Coal,  Pittsburgh 


Ft.  in. 
1 8 


207 


30 
10 
1 8 


250  4 
F 


'lG.  24. — Section  ;it. 
Burning  Springs 
W.  Va, 


Total 


White.  1 


SECTION  AT  ANTIQUITY,  OHIO. 


53 


Both  here  and  all  along  the  Volcano  anticline  the  Pittsburgh  coal 
is  very  poorly  developed,  as  shown  in  this  and  the  previous  section, 
and  it  is  frequently  absent  entirely. 

Section  on  Leading  Creelc , West  Virginia.—  Near  Leading  Creek  post- 
office,  at  the  eastern  edge  of  Gilmer  County,  West  Virginia,  this  series 
shows  thus  (Pig.  25) : 


Fig.  25.— Section  on 
Leading  Creek,  W.Va. 


Leading  Creelc , Gilmer  County , West  Virginia. 


[See  map,  P j.] 

Feet. 

1.  Waynesburg  coal  horizon  (absent) 0 

2.  Shales 10 

3.  Limestone,  brecciated 3 

4.  Shales  and  concealed ».  35 

5.  Sandstone,  yellow,  massive,  soft, pebbly 40 

6.  Shales 10 

7.  Limestone,  impure 2 

8.  Shales 40 

9.  Sandstone,  massive 40 

10.  Shales 55 

| Coaly  shales . . 2'  0"  1 
| Clay 0'  10"  1 

11. Coal,Pittoburgh...(g»^f»al::;»;  «;![ 8 

! Bony  slate o'  4"  |~ 

[ Coal 2'  0"J 

Total 243 


Section  at  Antiquity , Ohio. — Along  the  Ohio  River,  below  where  the 
Volcano  arch  crosses,  the  Upper  Coal  Measures  again  plunge  under 
water  level,  and  do  not  emerge  again  till  we  come  to  the 
vicinity  of  Antiquity,  Meigs  County,  Ohio,  100  miles  be- 
low. A shaft  to  the  Pittsburgh  bed  (130  feet  under  river 
level),  taken  in  connection  with  the  surface  exposures 
there,  reveals  the  following  succession  (Fig.  26) : 

Antiquity , Meigs  County,  Ohio. 

[See  map,  P e.] 

Ft.  in. 

L Waynesbnrg  coal  (absent) 0 

2.  Shales  and  sandstones 172 

3.  Sandstone,  massive,  Pittsburgh 70 

4.  Shales,  with  fossil  plants 10 

(Coal 2'  G") 

5.  Coal,  Pittsburgh < Slate O'  2"  > 5 g 

(Coal 3'  0") 

Total 257  8 


Fig.  26.  — Section 
at  Antiquity,  Ohio. 


Section  at  Hartford  City , West  Virginia,— Six  miles  below  the  shaft 
at  Antiquity,  and  in  the  vicinity  of  Hartford  City,  the  Pittsburgh  coal 


54 


THE  NORTHERN  BITUMINOUS  COAL  FIELD. 


[BULL.  65. 


comes  above  water  level.  In  the  steep  bluffs  above  Hartford  the  fol- 
lowing succession  (Fig.  27)  was  observed  : 


Hartford  City,  Mason  County , West  Virginia . 


70 


[See  map,  P d.] 

Ft.  in. 

1.  Waynesburg  coal  (absent) 0 

2.  Red  shale  10 

3.  Shale,  gray 5 

4.  Sandstone 6 

5.  Shales,  brown,  sandy 10 

6.  Shales,  red 2 

7.  Concealed 14 

8.  Red  shale,  with  limestone  nodules 10 

9.  Sandstone 20 

10.  Shales,  variegated  with  limestone  nodules  near  base 28 

11.  Concealed... - 20 

12.  Red  shale 5 

13.  Concealed 20 

14.  Shale,  red 15 

15.  Sandstone,  massive,  Pittsburgh 70 

16.  Shales,  gray,  fossil  plants 15 

17.  Coal,  Pittsburgh 5 6 

Total 255  6 


i 

Fig.  27. — Section  at 
Hartford  City, 

W.Va. 

Section  at  Arbuckle , West^  Virginia.— In  the  vicinity  of  Arbuckle, 
Mason  County,  West  Virginia,  on  the  Great  Kanawha  River,  and  18 
miles  above  its  mouth,  the  Waynesburg  coal  makes  its  appearance  in 
the  section.  Here  the  following  structure  (Fig.  28)  was  obtained  for 
the  series,  by  combining  the  surface  exposures  with  the  record  of  a 
boring  made  by  Mr.  Craig : 


Arbuckle,  Mason  County,  West  Virginia. 


[See  map,  Q e.) 


1.  Waynesburg  coal 


f Coal,  slatv 

..O' 

10" 

| Coal,  sulphurous . 

..O' 

8" 

<(  Shale,  dark 

..0' 

5" 

| Coal,  good 

..O' 

8" 

( Coal,  slaty 

..0' 

5" 

2.  Shales,  sandstone,  and  concealed 

3.  Sandstone,  blue 

4.  Shales,  red 

5.  Sandstone,  blue,  hard 

6.  Variegated  shales 

7.  Coal,  Sewickley 

8.  Sandstone 

9.  Shales,  red 

10.  Shales,  variegated 

11.  Fire  clay,  impure  (Redstone  coal) 

12.  Sandstone,  coarse,  white,  Pittsburgh 

13.  Fire  clay  and  shale  with  a little  slaty  coal  at  bottom,  Pittsburgh. 


Ft. 


150 

4 

2 

14 

8 

1 

6 

4 

48 

2 

29 

10 


Total . 


Fig.  28.— Sect 
at  Arbuckle, 
281  Va. 


ion 
, W. 


Here  there  is  practically  no  merchantable  coal  in  the  whole  series, 
since  the  Waynesburg  bed,  although  3 feet  thick,  is  poor  and  slaty. 


WHITE.] 


SECTION  OPPOSITE  WINFIELD,  W.  VA.  55 

The  locality  is  near  the  center  of  the  deepest  portion  of  the  Appalachian 
trough,  and  the  horizon  of  the  Pittsburgh  coal  is  90  feet  under  the  Ka- 
nawha. A hole  was  drilled  as  a test  for.  this  coal,  but  the  result  proved 


only  a trace  of  it  present. 

Section  at  mouth  of  Big  Hurricane  Creek , Putnam  County , West  Vir- 
ginia.— Southward  up  the  Kanawha  River  from  Arbuckle,  the  locality 
of  Section  28,  the  rocks  rise  and  the  entire  series  comes  above  water 


level  at  the  mouth  of  Big  Hurricane  Greek,  in  Putnam  County.  Here, 
32  miles  from  the  mouth  of  the  Big  Kanawha,  the  fol- 
lowing succession  may  be  seen  (Fig.  29) : 


mm 


-"••-••I 


TfsYVtYVYYY. 


Mouth  of  Big  Hurricane  Creek,  Putnam  County,  West  Virginia. 

[See  map,  R d.] 

Ft.  in. 

1.  Waynesburg  coal  (absent) - 0 

2.  Shales,  red  and  sandy 35 

3.  Sandy  shales 20 

4.  Sandstone,  massive . . 30 

5.  Coal,  Uniontown  0 G 

6.  Red  shales,  with  limestone 10 

7.  Shales,  sandy 10 

8.  Concealed 10 

9.  Shales,  sandy 10 

10.  Concealed  and  red  shales 20 

11.  Sandstone,  massive 20 

12. '  Concealed 20 

13.  Sandstone,  massive 35 

14.  Shale,  with  iron  ore 12 

15.  Sandstone 18 

[Coal 0'  10"  1 

Shales 5'  0"  | 

16.  Coal,  Pittsburgh,  roof <j  l^dston?. ! ! 1'  8" 

I Slate,  black  . . 2'  0" 

(Fireclay V 3' 


11'  9") 
I 
I 


15  8 


Fig.  29. — Section  at 
mouth  of  Big  Hurri- 
cane Creek,  W.  Va. 


C Coal 3'  3")  1 

Coal,  Pittsburgh,  main  bench.  < Slate 0'  2"  > 3'  11"  J 

l Coal 0'  6"  S 

Total 266  2 


The  Pittsburgh  coal  is  patchy  all  through  this  region, 
being  workable  on  some  farms  and  absent  on  others. 

Section  opposite  Winfield , West  Virginia. — As  showing 
the  unreliable  character  of  the  coals  in  this  series  along 
this  portion  of  the  Kanawha,  the  section  (Fig.  30)  of  the 
rocks  opposite  Winfield,  Putnam  County,  5 miles  above 
Big  Hurricane,  is  given  : 

Opposite  Winfield,  Putnam  County,  West  Virginia. 

[See  map,  So.] 


Ft. 

1.  Waynesburg  coal  (absent) 0 

2.  Shales,  red,  with  limestone  nodules 5 

3.  Sandstone,  shaly 10 

4.  Concealed 10 

5.  Red  shale 10 

6.  Sandstone,  flaggy 30 

7.  Red  shales,  with  limestone 10 

8.  Sandstone,  shaly 20 

9.  Red  shale - 25 

10.  Sandstone,  shaly - 10 

11.  Red  shales 10 

12.  Sandstone,  flaggy - 10 

13.  Concealed 10 

14.  Red  shale,  with  limestone  nodules  near  base 15 

15.  Sandstones,  red,  and  gray  shales 75 

16.  Fire  clay,  place  for  Pittsburgh  coal  — 0 


Total 250 


Fig.  30. — Section 
opposite  Win* 
lield,  W.  Va. 


56 


THE  NORTHERN  BITUMINOUS  COAL  FIELD. 


[BULL.  65. 


This  section  was  measured  in  the  steep  hill  at  Red  House  Station,  on 
the  Kanawha  and  Ohio  Railroad,  and,  as  may  be  seen,  the  series  does 
not  there  contain  any  coal  whatever. 

Section  near  Raymond  City,  West  Virginia.—  Further  up  the  Kanawha 
the  Pittsburgh  coal  again  comes  in,  and  the  follow- 
ing structure  (Fig.  31)  is  found  in  the  vicinity  of 
Raymond  City,  6 miles  above  Winfield  : 


30' 


Near  Raymond  City , Putnam  County , West  Virginia. 

[See  map,  S e,] 

Ft.  in. 

1.  TVaynesburg  coal  (absent) 0 

2.  Concealed,  with  red  shale  60 

3.  Red  shale 30 

4.  Sandstone,  gray,  micaceous 4 

5.  Limetone,  in  red  shale 5 

6.  Red  shale 15 

7.  Sandy  shale,  gray 30 

8.  Shale,  red 40 

9.  Sandy  shales,  yellowish  gray 45 

10.  Black  shale,  Redstone  coal 2 

11.  Sandstone,  Pittsburgh 40 

12.  Shales 10 

( Coal 0'  4' 

j Shale 0'  4 

13.  Coal,  Pittsburgh,  roof -i  g^Je ; ; ; ; ; ; 

| Coal,  slaty...  V 0' 

[Fine  clay V 6' 


Fig.  31.  — Section  near 
Raymond  City,  W.  Va. 


L Coal,  good 

14.  Coal,  Pittsburgh,  main  bench.  { ~m 


0" 

Slate!  1 0-  £ 

(Coal,  slaty... 0'  10 


i) ' 

■s 


6'  10*' 


10  7$ 


Total 291  7* 


Section  in  vicinity  of  Western  Port , Maryland. — In  the  Cumberland  or 
Georges  Creek  basin,  the  Upper  Coal  Measures  ex- 
hibit the  following  structure  (Fig.  32),  as  observed 
in  the  vicinity  of  Western  Port,  Maryland : 

Vicinity  of  Western  Port,  Alleghany  County,  Maryland. 

[See  map,  N p.] 

Ft.  in. 

1.  Waynesburg  coal  (not  seen) 0 

2.  Concealed  and  shales 130 

3.  Coal,  Sewickley 5 

4.  Shales  and  concealed * 115 


5.  Coal,  Pittsburgh,  roof 


[Coal 

. 0' 

8"' 

j 

] Shale 

. 4' 

0" 

> 6'  8 " 1 

) Coal 

0" 

1 Shale 

. 1' 

0"  J 

1 

[Coal 

.10' 

0"1 

1 

V 

Slate 

0' 

2" 

( 

| Coal 

. 0' 

9" 

^ Slate 

. 0' 

> 13'  7 i"J 

1 Coal 

. 2' 

0”  1 

| Black  slate  

. 0' 

6"  I 

[ Soft  coaly  shale 

. O' 

2"  J 

1 

20  31 


Total 270  3J 


Fig.  32. — Section 
near  W estern  Port,  Md. 


WHITER 


THE  UPPER  COAL  MEASURES. 


57 


From  the  foregoing  sections  it  will  be  perceived  that  the  beds  in  the 


Upper  Coal  Measures  which  have 
scending  order  as  follows  : 

Waynesburg  coal. 

Browntown  sandstone. 

Little  Waynesburg  coal. 
Waynesburg  limestone. 

Uniontown  sandstone. 

Uniontown  coal. 

Uniontown  limestone. 

Great  limestone. 


received  distinct  names  are  in  de- 


Sewickley  sandstone. 
Sewickley  coal. 
Sewickley  limestone. 
Redstone  coal. 
Redstone  limestone. 
Pittsburgh  sandstone. 
Pittsburgh  coal. 


These  several  beds  we  shall  now  notice  more  in  detail. 


CHARACTERISTIC  HORIZONS. 


THE  WAYNESBURG  COAL. 


This,  the  highest  member  of  the  series,  is  generally  quite  persistent 
around  the  northern  end  of  the  coal  field,  but  followed  southward 
through  West  Virginia  it  soon  becomes  patchy  and  interrupted,  so  that 
beyond  the  line  of  Marion  County  the  coal  is  only  occasionally  present 
along  the  eastern  and  central  portions  of  the  Upper  Coal  Measure  belt, 
its  horizon  being  frequently  occupied,  as  at  Harrisville,  Ritchie  County 
by  a brecciated  limestone. 

On  the  Great  Kanawha  this  coal  occurs  near  the  center  of  the  Appa- 
lachian trough  over  a small  area  in  the  vicinity  of  Arbuckle,  and  its 
structure  there  is  given  in  Section  28. 

Along  the  western  side  of  the  field,  down  the  Ohio  River  and  across 
southern  Ohio,  this  coal  is  fairly  persistent.  It  dips  under  the  Ohio 
River  at  New  Martinsville,  but  rises  to  daylight  again  near  St.  Mary’s, 
where  it  is  only  1 to  3 feet  thick,  and  quite  sulphurous. 

In  the  Macksburg  oil  region  it  is  the  principal  bed,  according  to  the 
Ohio  geologists,  and  has  a thickness  of  4 feet. 

This  coal  is  almost  universally  double,  being  separated  into  two  layers 
by  a division  of  shale  and  slate.  This  is  so  common  at  the  northern  end 
of  the  field  that  it  is  known  there  as  the  “horse-back”  vein.  In  Mo- 
nongalia and  Greene  Counties  the  bed  is  often  8 to  10  feet  thick  and 
separated  into  three  layers,  the  upper  division  of  slate  being  very  fos- 
siliferous,  and  often,  as  at  Cassville,  West  Virginia,  containing  many 
insect  remains,  together  with  fossil  plants. 

The  coal  from  this  bed  is  usually  rather  hard,  and  comes  out  in  large 
blocks ; but  it  frequently  contains  injurious  quantities  of  sulphur.  This 
renders  it  unfit  for  smithing,  as  well  as  for  the  manufacture  of  coke  and 
gas,  but  it  is  generally  a useful  fuel  for  steam  and  domestic  jmrposes. 


IRON  ORE. 

The  shales  which  underlie  the  Waynesburg  coal  sometimes  contain 
a considerable  quantity  of  iron  nodules,  and  they  were  once  mined  in 


58 


THE  NORTHERN  BITUMINOUS  COAL  FIELD. 


[BULL.  66. 


Morgan  Township,  Greene  County,  Pennsylvania,  and  used  in  manu- 
facturing iron.  The  same  ore  occurs  near  Bethel  Church,  Cass  District, 
Monongalia  County,  at  15  to  20  feet  below  the  coal. 

THE  BROWNTOWN  SANDSTONE. 

In  many  portions  of  Marion  and  Harrison  Counties,  West  Virginia, 
the  interval  beginning  5 to  10  feet  below  the  Waynesburg  coal  is  occu- 
pied by  a hard,  gray,  massive  sandstone,  20  to  35  feet  thick.  It  is 
finely  exposed  along  the  bed  and  bluffs  of  Ten  Mile  Creek,  at  and  below 
Browntown,  Harrison  County,  West  Virginia,  and  has  been  designated 
from  that  locality.  The  deep,  rocky  cuts  along  the  Baltimore  and  Ohio 
liailroad,  beginning  1 mile  east  of  Mannington,  Marion  County,  and 
extending  to  the  mouth  of  Mod’s  Run,  are  all  in  this  sandstone.  It  is 
sometimes  called  the  “ Gilboy  ” sandstone,  from  a rocky  cut  of  that 
name  near  Mannington.  This  is  nearly  always  a water-bearing  stratum, 
and  the  oil  wells  of  Marion  County  have  to  be  cased  below  this  rock  in 
order  to  shut  off  the  fresh  water. 

THE  LITTLE  WAYNESBURG  COAL. 

At  many  localities  around  the  northern  end  of  the  Upper  Coal  Meas- 
ure area  a thin  streak  of  coal  or  bituminous  slate  occurs  at  25  to  40 
feet  below  the  Waynesburg  coal,  and  it  was  termed  the  Little  Waynes- 
burg coal  by  Prof.  Stevenson.  It  seldom  exceeds  1 foot  in  thickness, 
and  is  of  no  economic  importance.  It  is  usually  separated  from  the 
main  coal  above  by  shales  and  sandy  beds,  and  should  probably  be 
regarded  as  an  offshoot  from  the  Waynesburg  coal  proper.  It  is  seldom 
seen  south  from  the  Pennsylvania  line,  though  it  occurs  along  the  Ohio 
River  at  several  places. 

THE  WAYNESBURG  LIMESTONE. 

Directly  under  the  last  described  stratum  there  occurs  a limestone 
of  very  wide  distribution.  Its  place  is  generally  about  40  feet  below 
the  Waynesburg  coal,  though  sometimes  it  is  less,  and  occasionally  a 
few  feet  more.  It  is  usually  of  a dark  gray  color,  and  several  of  the 
layers  make  excellent  lime  for  agricultural  and  building  purposes.  The 
thickness  in  Pennsylvania  and  northern  West  Virginia  is  seldom  less 
than  8 feet,  and  frequently  double  that,  but  south  westward,  toward  the 
Great  Kanawha  region,  the  limestone  disappears  entirely. 

THE  UNIONTOWN  SANDSTONE. 

At  60  to  75  feet  below  the  top  of  the  series  there  frequently  occurs 
a massive,  gray  sandstone  whose  horizon  comes  immediately  above  the 
Unioutown  coal;  and  hence,  although  the  stratum  in  question  is  not 
prominent  at  Uniontown,  it  has  been  designated  from  its  relations  to 
the  underlying  coal. 

The  rock  has  occasionally  been  mistaken  for  the  Waynesburg  sand- 
stone, which  belongs  nearly  100  feet  above.  It  is  well  exposed  at  Bob- 


WHITE.] 


THE  UPPER  COAL  MEASURES. 


59  l 

town,  Greene  County,  Pennsylvania,  where  it  crowns  the  summit  of  the 
hill  overlooking  Dunkard  Greek  as  a bold  cliff. 

In  the  Georges  Creek  coal  field  a massive  sandstone  occurs  250  feet 
above  the  Pittsburgh  coal,  and  it  was  once  referred  by  the  writer  to 
the  Uniontown  horizon  under  the  name  of  “ Westernport  sandstone,” 
but  subsequent  study  seems  to  place  it  in  the  horizon  of  the  Waynes- 
burg  sandstone. 

THE  UNIONTOWN  COAL. 

This  bed  underlies  the  Waynesburg  coal  by  an  interval  of  80  to  100 
feet,  and  is  of  economic  importance  only  in  Fayette  and  Washington 
. Counties,  Pennsylvania.  It  was  named  by  Kogers  from  Uniontown, 
Fayette  County,  where  it  is  well  exposed.  The  thickness  seldom  ex- 
ceeds 3 feet,  even  in  the  region  of  its  best  development,  and  the  coal 
has  never  been  used  except  for  domestic  purposes,  since  it  is  usually 
neglected  for  the  great  Pittsburgh  bed  below.  It  often  contains  a 
clay  or  slate  parting  near  the  center,  4 to  G inches  thick,  and  is  rather 
too  rich  in  ash  for  a first-class  fuel. 

Southward  from  Fayette  County,  through  Greene,  Monongalia,  Mar- 
ion, and  Harrison,  this  coal  thins  away  to  a bed  of  black  slate  mixed 
with  slaty  coal  that  is  often  rich  in  fish  remains  and  bivalve  crusta- 
ceans, which  may  be  found  in  abundance  near  Davistown,  Greene 
County,  Pennsylvania. 

Along  the  Ohio  Eiver  at  Wheeling,  Bellaire,  Clarington,  and  other 
points,  this  bed  is  sometimes  represented  by  a thin  streak  of  black  slate 
or  coal.  In  the  Salisbury  basin  of  Pennsylvania  it  is  recognized  by 
Messrs.  Platt,  and  is  there  over  3 feet  thick,  with  slate  near  center. 

THE  UNIONTOWN  LIMESTONE. 

To  the  division  of  the  u Great”  Limestone  which  immediately  under- 
lies the  last  described  coal  bed,  Dr.  Stevenson  gave  the  name  Union- 
town,  since  it  seems  to  be  fairly  well  separated  from  the  great  mass  of 
limy  deposits  below.  This  division  is  usually  10  to  15  feet  thick,  though 
occasionally  it  surpasses  these  figures.  The  rock  is  frequently  impure 
and  of  a huffish  color,  being  magnesian,  and  occasionally  a good  cement 
rock,  as  at  Uniontown,  Pennsylvania.  This  is  the  only  member  of  the 
“ Great”  Limestone  which  appears  to  be  persistent  from  the  Pennsyl- 
vania line  southward  across  West  Virginia  to  the  Big  Kanawha  River, 
since  an  impure  limestone  only  2 to  5 feet  thick  occurs  at  this  horizon 
in  the  vicinity  of  Raymond  City  and  other  points  in  that  region. 

In  the  Salisbury  basin  this  limestone  occurs  only  160  feet  above  the 
Pittsburgh  coal,  and  is  10  to  12  feet  thick,  according  to  Platt. 

THE  “ GREAT  ” LIMESTONE. 

This  name,  given  by  Rogers,  is  generally  applied  to  all  of  the  great 
mass  of  lime  deposits  which  intervene  between  the  Uniontown  and 
Sewickley  coals,  though,  as  already  stated,  the  name  Uniontown  is  now 
given  to  the  uppermost  division  of  the  same. 


60 


THE  NORTHERN  BITUMINOUS  COAL  FIELD. 


[bull.  65. 


At  many  localities  in  Greene,  Washington,  Fayette,  and  Monongalia 
Counties  there  are  nearly  160  feet  of  limestones  and  limy  shales  at  this 
horizon,  and  the  same  beds  hold  their  place,  though  with  diminished 
thickness,  across  to  the  Ohio  Eiver  at  Wheeling.  Westward  and  south- 
ward, however,  from  Ohio  and  Marion  Counties,  these  limestones  disap- 
pear very  rapidly,  so  that  at  Clarksburg  on  the  one  hand,  and  west-  * 
ward  through  Ohio  on  the  other,  they  have  practically  disappeared, 
and  in  their  stead  we  find  shales,  gray  at  first,  but  gradually  getting 
reddish  toward  the  Little  Kanawha  Eiver  and  the  western  margin  of 
their  outcrop  in  Ohio.  On  the  Big  Kanawha  much  red  shale  occurs  at 
this  horizon.  These  limestones  are  of  different  qualities,  some  of  the 
layers  being  quite  pure  and  forming  good  fluxes  for  iron,  while  others 
are  magnesian  and  make  excellent  hydraulic  cements. 

The  only  fossils  ever  seen  in  any  of  these  limestone  beds  are  fish  re- 
mains and  minute  ostracoids. 

THE  SEWICKLEY  SANDSTONE. 

At  many  localities  where  the  u Great v Limestone  is  well  developed 
there  are  no  other  beds  except  limestones  and  shales  in  all  of  the  inter- 
val between  the  Uniontown  and  Sewickley  coals,  but  in  other  regions 
a sandstone  frequently  makes  its  appearance  just  above  the  Sewickley 
coal.  This  has  been  called  the  Sewickley  sandstone,  and  while  it  is 
often  flaggy,  yet  again  it  becomes  massive,  and  even  pebbly,  varying 
in  thickness  from  20  to  60  feet.  Its  massive  character  is  well  shown 
along  the  Monongahela  Eiver  between  Morgantown  and  Fairmont,  in 
the  vicinity  of  the  Big  Falls. 

THE  SEWICKLEY  COAL. 

Directly  under  the  Sewickley  sandstone,  or  in  its  absence  the  u Great 79 
Limestone,  there  comes  the  Sewickley  coal,  a bed  which  is  widely  per- 
sistent, though  the  area  where  it  is  valuable  is  not  so  large. 

The  bed  attains  its  maximum  thickness  and  importance  along  the 
Monongahela  Eiver  in  Greene,  Monongalia,  and  Marion  Counties,  beiug 
there  5 to  6 feet  thick,  with  only  one  slate  parting  of  2 to  3 inches  near 
the  center.  The  coal  is  generally  high  in  both  ash  and  sulphur,  but  is 
open-burning  and  makes  a rather  fair  domestic  fuel. 

The  following  represents  the  general  structure  of  this  bed  along  the 
Monongahela  Eiver  in  Marion  and  Monongalia  Counties : 

Ft.  in. 


Coal 2 8j 

Slate 0 2}  5'  6" 

Coal 2 8 j 


Followed  down  the  Monongahela  Eiver,  the  bed  retains  about  the 
same  structure  as  far  as  the  mouth  of  Whitely  Creek,  Greene  County, 
Pennsylvania,  when  the  slate  partings  thicken  up,  and  new  ones  come 
in  and  dissipate  the  coal  in  several  thin  layers  through  25  feet  of  rock 


geological  survey  Bulletin  no.  65  Rl.  Vii 


UPPER  COAL  MEASURES  AT  POINT  PLEASANT,  WEST  VIRGINIA,  SHOWING  RUGGED  CHARACTER  OF  THE  T_ . _GRAPHY. 


THE  LIBRARY 
OF  THE 

UNIVERSITY  OF  ILLINOIS 


WHITE.] 


THE  UPPER  COAL  MEASURES. 


61 


material,  and  from  thence  on  down  that  river  it  is  of  no  importance. 
But  followed  in  the  other  direction,  up  the  Monongahela,  this  bed  holds 
a thickness  of  5 to  6 feet  through  Marion  County  until  the  Harrison 
County  line  is  approached,  when  it  again  splits  up  into  three  or  four  di- 
visions separated  by  several  feet  of  shales  and  slates,  and  when  Clarks- 
burg is  reached  there  remains  only  1 foot  of  coal  at  this  horizon  (Sec- 
tion 18),  which  soon  disappears  entirely  toward  the  southwest. 

From  the  Monongahela  region  this  coal  dips  down  westward  under 
the  great  mantle  of  Permo-Carboniferous  beds,  and  when  it  reappears 
on  the  Ohio  River,  in  the  vicinity  of  Wheeling  (Section  19),  Bellaire 
(Section  20),  and  Pipe  Creek  (Section  22),  we  find  it  split  up  again  into 
three  or  four  layers,  and  the  separating  slates  several  feet  thick,  thus 
giving  the  whole  bed  a thickness  of  20  to  30  feet,  with  the  main  coal 
layer  at  the  top. 

This  uppermost  division  of  the  Sewickley  is  separated  from  the  Pitts- 
burgh below  by  an  interval  of  80  to  100  feet,  and  attains  considerable 
importance  in  the  counties  of  Belmont,  Harrison,  Guernsey,  Monroe, 
Morgan,  Muskingum,  Noble,  etc.,  and  has  there  been  mined  under  a 
variety  of  names,  among  which  are  “ Upper  Barnesville,”  “ Upper  Bel- 
laire,” “ Cumberland,”  u Meigs  Creek,”  and  several  others.  Prof.  Orton, 
while  intimating  its  identity  with  the  Sewickley  of  Pennsylvania  (Vol. 
Y,  page  1059,  Ohio  Geology),  prefers  to  call  it  by  the  name  of  Meigs 
Creek,  from  a stream  in  Morgan  County  along  which  it  is  well  devel- 
oped. 

Throughout  much  of  this  Ohio  region  the  coal  is  3 to  4J  feet  thick, 
and  nearly  always  has  a clay  or  bony  streak  near  its  center.  It  also 
frequently  has  a rider  coal  in  the  roof,  and  the  entire  bed  is  rather  rich 
in  ash  and  sulphur,  according  to  Orton. 

In  Fayette  County,  Pennsylvania,  the  Sewickley  coal  has  a thickness 
of  4 to  5 feet  through  several  townships,  according  to  Stevenson,  but 
northward  through  Westmoreland  it  thins  down  and  is  unimportant. 
It  is  scarcely  known  in  the  Ligonier  basin,  but  in  that  of  Salisbury  is 
2 feet  thick  and  90  feet  above  the  Pittsburgh. 

In  the  Georges  Creek  basin  of  Maryland  and  West  Virginia  the  bed 
is  5 to  7 feet  thick,  90  to  115  feet  above  the  Pittsburgh,  and  an  excellent 
coal  for  steam  purposes. 

The  oil-borings  across  Monongalia  and  Marion  Counties  reveal  this 
coal  present  in  good  thickness  10  to  15  miles  west  from  the  Mononga- 
hela River,  and  100  to  110*  feet  above  the  Pittsburgh  coal.  The  oil 
drillers  usually  call  it  the  “Mapletown”  coal,  from  a locality  in  Greene 
County  where  it  is  mined. 

THE  SEWICKLEY  LIMESTONE. 

The  interval  between  the  Sewickley  coal  and  the  one  next  below  is 
•often  occupied  largely  by  limestone,  especially  in  Greene,  Fayette, 
Washington,  Monongalia,  and  Marion  Counties,  and  to  the  one  which 


62 


THE  NORTHERN  BITUMINOUS  COAL  FIELD. 


BULL.  65. 


comes  next  below  the  coal  Messrs.  Platt  have  given  the  name  Be- 
wick ley.  It  has  also  been  termed  the  Fishpot  Limestone  by  Ste- 
venson, from  a small  stream  in  Washington  County.  I have  deemed  it 
preferable  to  apply  the  name  Sewickley  to  the  whole  limestone  group 
which  lies  between  the  Sewickley  and  Redstone  coal  beds.  This  inter- 
val is  40  to  60  feet  thick  and  sometimes  contains  two  beds  of  sandstone 
intercalated  with  the  limestones.  Along  the  Monongahela  River  iu. 
Greene,  Monongalia,  and  Marion  Counties,  these  limestones  are  well 
developed,  and  many  of  the  layers  furnish  excellent  lime  for  mortar  and 
agricultural  uses,  while  near  the  base  of  the  group  occur  some  excellent 
limestone  flags  at  Laurel  Point,  Monongalia  County. 

The  only  fossils  ever  noted  in  these  beds  are  minute  fresh- water  types. 

These  limestones  disappear  southward  from  Harrison  Qounty,  West 
Virginia,  there  being  only  9 feet  of  them  in  the  Clarksburg  section,  and 
none  on  the  Little  and  Big  Kanawha  Rivers.  The  same  thing  takes 
place  in  Ohio,  westward  from  Washington  County,  the  interval  being- 
occupied  by  shales  and  sandstones. 

In  Pennsylvania  this  Sewickley  limestone  holds  a prominent  place 
eastward  from  Washington  and  Greene,  through  Fayette,  Westmore- 
land, and  Somerset  Counties. 

TftE  REDSTONE  COAL. 

In  Fayette  County,  Pennsylvania,  a small  coal  was  found  cropping 
out  along  Redstone  Creek,  at  an  interval  of  40  to  45  feet  above  the 
Pittsburgh,  and  this  was  named  from  that  stream  by  the  geologists 
of  the  First  Pennsylvania  Geological  Survey. 

Monongalia  is  the  only  county  in  West  Virginia  where  this  bed  is 
workable,  it  being  there,  on  Scott’s  and  Robinson’s  Runs,  4 to  5 feet 
thick  and  of  fair  quality,  though  having  rather  too  much  sulphur  and 
ash  for  manufacturing  purposes.  It  is  also  workable  in  several  town- 
ships of  Fayette  and  Westmoreland,  being  3 to  4 feet  thick.  In  the 
Salisbury  basin  of  Somerset  County,  Messrs.  Platt  identify  the  Red- 
stone coal  as  a slaty  bed,  4 feet  thick,  at  45  feet  above  the  Pittsburgh. 
It  has  not  been  reliably  reported  from  the  Georges  Creek  field  unless 
it  be  represented  by  one  of  the  rider  layers  in  the  roof  of  the  Pitts- 
burgh bed. 

In  the  vicinity  of  Wheeling,  Bellaire,  and  other  points  on  the  Ohio 
River,  this  bed  is  only  a few  inches  thick,  never  becoming  workable 
anywhere  in  Ohio. 

Through  central  West  Virginia,  beyond  the  Little  Kanawha,  its  pres- 
ence is  unknown  except  by  a bed  of  black  slate  which  is  occasionally 
seen  at  this  horizon. 

THE  REDSTONE  LIMESTONE. 

At  many  localities  along  the  Monongahela  River  in  Harrison,  Marion, 
Monongalia,  Greene,  Washington,  Fayette,  and  Westmoreland  Coun- 
ties, there  occurs  a bed  of  limestone  often  10  to  20  feet  thick,  and  im- 


WHITE.  ] 


THE  UPPER  COAL  MEASURES. 


63 


mediately  underlying  the  Redstone  coal.  From  this  latter  fact  it  was 
termed  the  Redstone  limestone  by  Messrs.  Platt,  who  find  the  same 
bed  in  Somerset  County,  40  to  45  feet  above  the  Pittsburgh  coal.  It 
often  contains  several  layers,  which  make  fairly  good  lime  for  many 
purposes,  and  is  occasionally  used  for  flux  in  iron  furnaces. 

This  limestone  is  also  in  great  force  in  the  vicinity  of  Wheeling,  Bel- 
laire,  and  vicinity,  where  it  occupies  nearly  the  entire  interval  between 
the  Redstone  and  Pittsburgh  coals,  and  is  extensively  quarried  as  a 
flux  for  the  furnaces  there. 

It,  like  all  the  other  limestones,  disappears  southwestward  through 
West  Virginia,  and  is  not  known  beyond  the  Little  Kanawha  River. 

THE  PITTSBURGH  SANDSTONE. 

Very  frequently,  and  especially  when  the  Redstone  limestone  is  well 
developed,  there  is  nothing  but  shales  intervening  between  it  and  the 
Pittsburgh  coal,  but  when  the  limestone  is  absent,  or  but  poorly  repre- 
sented, there  is  often  present  a coarse,  massive  sandstone  immediately 
above  the  Pittsburgh  coal,  and  to  this  Mr.  H.  D.  Rogers  long  ago  gave 
the  name  of  Pittsburgh  sandstone.  It  varies  in  thickness  from  25  up 
to  70  feet,  and  is  usually  coarse,  friable,  and  often  pebbly.  Good  build- 
ing stone  has  never  been  obtained  from  it,  since  it  yields  so  readily  to 
atmospheric  agencies. 

This  rock  is  especially  massive  in  the  vicinity  of  Hartford  City, 
Pomeroy,  and  other  contiguous  regions,  and  the  same  may  be  said  of 
the  eastern  line  of  its  outcrop  from  Pennsylvania  clear  across  West 
Virginia  to  the  Kentucky  border. 

In  the  Georges  Creek,  Salisbury,  and  Ligonier  basins,  however,  this 
rock  makes  but  little  show  in  the  topography,  its  place  being  occupied 
by  soft  shales. 

THE  PITTSBURGH  COAL. 

The  last  and  lowest  member  of  the  Upper  Coal  Measures  is  the  cele- 
brated Pittsburgh  bed,  the  most  important  mineral  deposit  of  the  Ap- 
palachian field. 

It  was  formerly  thought  that  this  coal  bed  was  entirely  persistent ; 
that  wherever  its  horizon  was  to  be  found,  there  the  coal  might  be 
expected  with  absolute  certainty.  This  generalization,  however,  was 
founded  on  data  obtained  only  from  the  northern  half  of  its  area.  In 
Pennsylvania,  for  instance,  no  area  has  yet  been  discovered  where,  at 
the  proper  geological  horizon  for  this  bed,  it  does  not  exist.  Even  in 
central  Greene,  at  a depth  of  1,500  feet  below  the  Permo-Carboniferous 
summits,  the  drill  of  the  petroleum  seeker  invariably  finds  this  coal 
bed,  while  the  isolated  peak  of  Round  Top,  in  the  Broad  Top  coal  basin 
of  Bedford  County,  50  miles  distant  from  any  other  outcrop  of  the  coal, 
likewise  contains  it.  But  when  we  pass  southwestward  across  the  West 
Virginia  and  Ohio  coal  field,  Pennsylvania  conditions  of  course  continue 


64 


THE  NORTHERN  BITUMINOUS  COAL  FIELD. 


[bull.  65. 


for  many  miles,  but  ultimately  there  comes  a change,  and  when  we  look 
for  the  Pittsburgh  bed  it  is  gone,  or  so  reduced  in  thickness  that  the 
geologist  can  only  recognize  it  by  its  associated  rocks.  The  region  of 
country  covered  by  this  barren  area  is  quite  extensive,  and  seems  to 
be  rudely  coincident  with  the  line  of  the  Volcano  or  Burning  Springs 
anticlinal  of  West  Virginia. 

The  following  counties  in  that  State  have  the  coal  but  poorly  devel- 
oped or  wanting  at  the  horizon  where  it  belongs : Calhoun,  Boane, 
Wirt,  Kitchie,  Pleasants,  and  Wood.  This  belt  projected  northward 
through  Ohio  takes  in  the  counties  of  Washington,  Noble,  and  Mor- 
gan, in  all  of  which  the  coal  is  thin  or  wanting  altogether.  Thus  it 
happens  that  over  a belt  of  country  30  to  50  miles  wide,  and  running 
nearly  north  and  south  across  the  Appalachian  coal  field,  the  spread 
of  this  bed,  so  even  and  persistent  at  the  north,  is  here  irregular,  inter- 
rupted, and  wanting.  West  from  this  belt  the  coal  comes  in  again  and 
is  fairly  regular  in  parts  of  Kanawha,  Putnam,  and  Mason  Counties, 
east  from  the  Big  Kanawha ; but  west  from  that  stream  the  bed  is  thin, 
patchy,  and  of  little  importance  through  Cabell  and  Wayne,  til  bit  dis- 
appears from  the  center  of  the  great  Appalachian  trough  in  the  hilltops 
overlooking  the  Big  Sandy  River. 

In  Ohio,  also,  a considerable  area  of  this  coal  comes  in  west  from 
the  barren  belt,  and  extends  ‘through  Meigs  and  Athens  Counties  with 
fairly  good  thickness,  but  westward  from  them,  in  Gallia,  the  coal  is 
again  thin  and  uncertain. 

The  foregoing  sections,  Nos.  11  to  32  inclusive,  show  in  a general 
way  the  detailed  structure  of  the  Pittsburgh  coal,  so  that  oi  * a few 
others  need  be  given  in  this  connection  to  exhibit  its  structure  iu 
every  important  region  of  its  widely  extended  area. 

As  will  be  seen  from  these  sections,  the  coal  is  nearly  always  sepa- 
rated into  two  well  defined  portions  (the  roof  and  the  main  bench)  by 
a layer  of  clay,  and  there  are  often  several  divisions  of  the  rot  f,  as  also 
of  the  main  bench.  The  layers  of  coal  in  the  roof  are  usually  not  more 
than  1 to  1J  feet  thick,  and  separated  by  shales  of  about  the  same 
thickness,  while  the  divisions  of  slate  in  the  main  bench  are  mere  knife 
edges,  seldom  exceeding  an  inch  in  thickness  and  generally  not  more 
than  half  that  amount. 

Along  the  Monongahela  River,  two  of  these  slates  are  especially  con- 
stant, since  they  come  about  2J  to  3 feet  above  the  bottom  of  the  bed 
and  are  4 to  6 inches  apart.  They  are  usually  known  as  the  “ bearing 
in”  slates,  and  are  seldom  more  than  one-lialf  inch  thick.  Then  1 to  14 
feet  below  these  there  is  generally  another  thin  parting  of  slate  which 
runs  through  the  bed  with  great  persistency,  dividing  the  lower  portion 
into  two  layers  known  by  the  miners  as  the  “ brick”  coal,  and  “bot- 
tom ” coal.  Of  course  there  are  other  partings  which  occasionally  make 
their  appearance  in  the  bed  at  some  localities,  but  they  are  irregular 
and  not  persistent. 


THE  PITTSBURG  COAL  OUTCROP  NEAR  CONNELLSVILLE,  PENNSYLVANIA,  SHOWING  COLUMNAR  STRUCTURE  OF  TYPICAL  COKING  COAL. 


TKE  LIBRARY 
OF  THE 

UNIVERSITY  OF  ILLINOIS 


WHITE.  J 


SECTION  ON  FAIRFAX  KNOB,  W.  VA. 


65 


Section  at  Newburg , West  Virginia.— The  summits  around  Newburg, 
Preston  County,  West  Virginia,  catch  small  areas  of  this  bed  in  the 
syncline  between  the  Chestnut  Eidge  and  Laurel  Hill  anticlinals,  and 
the  coal  has  there  the  following  structure  : 


Ft.  in. 


Pittsburgh  sandstone 


Slaty  coal 0 

Shale 0 

Coal 0 

Shale  and  fire  clay 2 

Coal 9 

Slate 0 

Coal,  slaty 1 


9!Ft- 
» 4 
0.1 
0\ 

3^10 

6J 


in. 

31 


Ft. 

15 


Section  at  Copeman’s  Knob , West  Virginia. — In  the  next  trough  east  of 
the  Laural  Hill  anticlinal,  a small  isolated  area  of  the  Pittsburgh  coal 
is  caught  in  Copeman’s  Knob,  which  overlooks  Cheat  Eiver  at  the  foot 
of  Briery  Mountain,  near  Albrightsville,  Preston  County,  West  Vir- 
ginia, and  there  the  coal  shows  this  structure : 


f Shales 

I Coal 

j Slate 

Roof.  Coal,  slaty 

j Slate 

j Coal 

I Clay 

Main  coal,  partings  not  visible 


Ft.  iu. 


oi 

« 

4 ! Ft. 

2>  n 


6 I 

6j 


j Ft. 
V 19 


10  J 


Section  32  gives  the  structure  of  this  coal  still  farther  eastward  in 
the  Georges  Creek  basin,  and  it,  when  compared  with  the  Albright, 
Newburg,  and  Fairmont  (Sec.  17)  structures,  shows  a gradual  eastward 
thickening  of  the  bed  from  7 feet  on  the  Monongahela  to  20  at  many 
points  in  the  Georges  Creek  field. 

Section  at  Fairfax  Knob , Tucker  County , West  Virginia. — Near  the 
southern  end  of  the  Georges  Creek  basin,  at  the  head  of  the  North  Po- 
tomac Eiver,  a small  area  of  the  Pittsburgh  bed  is  caught  in  the  sum- 
mit of  Fairfax  Knob,  3,250  feet  above  tide,  and  20  miles  distant  from 
any  other  outcrop  of  the  coal.  The  main  portion  of  the  bed  is  here 
split  into  three  portions,  separated  by  several  feet  of  shales,  from  the 
thickening  up  of  the  parting  slates,  as  follows  : 

Ft.  in.  Ft. 


( Shales.. 
Roof . ) Coal  — 
( Shale... 

2 

0 l 

6 

ol 

Coal,  “breast”. 

, Coal 

) Slate  

8'  2"  \ 

O'  2“  V 9 

V 2"  ; 

5'  0“  \ 

4'  0"  >16 

v o#/  S 

4 

6 

Shales 

Limestone 

( Coal 

o l 

Shales 

Coal,  “brick”  .. 

< 

(I 

Fireclay  and  shales 

18 

0 

Coal,  “bottom,” 

slaty 

7 

OJ 

Bull.  G5 5 


66 


THE  NORTHERN  BITUMINOUS  COAL  FIELD. 


[HULL.  65. 


As  will  be  seen  from  the  above,  it  would  appear  that  the  three  main 
divisions  ot  the  Pittsburgh  bed,  viz,  “ breast,”  u brick,”  and  “ bottom,” 
are  here  separated  by  shales,  1G  and  18  feet  thick  respectively,  instead 
of  mere  partings  of  a fraction  of  an  inch,  as  on  the  Monongahela  and 
elsewhere,  thus  spreading  the  21  feet  of  coal  through  an  interval  of  55 
feet.  It  is  also  worthy  of  note  that  although  the  partings  have  here 
Increased  so  wonderfully,  yet  the  total  thickness  of  coal  remains  the 
same  as  in  the  central  part  of  the  Georges  Creek  Basin, 

In  the  vicinity  of  Glenville,  on  the  Little  Kanawha  Kiver,  this  coal 
is  4J  to  5 feet  thick,  with  a bony  streak  16  inches  below  the  top  of  the 
bed. 

The  structure  on  the  Big  Kanawha  is  given  in  Section  31. 

Section  at  Huntington , Cabell  County , West  Virginia. — In  the  summits 
of  the  hills  south  of  Huntington,  Cabell  County,  West  Virginia,  this 
coal  displays  the  following  structure  : 


Ft. 

Coal 0 

Clay 0 

Coal 3 

Slaty  coal 0 


in. 

6^1 


j Ft. 


6I 

2J 


The  farthest  point  to  the  southwest  that  this  bed  has  ever  been  seen 
is  in  the  summit  of  a hill  overlooking  the  Big  Sandy  Kiver,  10  miles 
above  its  mouth,  where  a small  patch  is  caught  in  the  center  of  the 
Appalachian  trough,  which,  rising  to  the  southwest,  carries  the  coal 
above  the  highest  hills  on  the  Kentucky  side  of  the  Big  Sandy.  The 
coal  is  here  3 feet  2 inches  thick  and  single  bedded,  or  with  only  faint 
partings. 

Section  at  Pomeroy , Meigs  County , Ohio. — At  Pomeroy,  Ohio,  the 
Pittsburgh  coal  shows  thus,  according  to  Prof.  E.  Lovejoy.  Ohio  Geo- 
logical Survey,  Vol.  VI,  page  636: 

In. 

Coal 8-14  "j 

Horn  coal 3 j Ft.  in. 

Coal . ..42-47  > 5 10 

Clay . 4 | 

Coal 7 J 

Section  on  Shade  Creek , Ohio. — In  the  Shade  Creek  coal  field  of  Meigs 
and  Athens  Counties,  Ohio,  Prof.  Lovejoy  finds  a well  developed  rider 
coal  12  to  20  feet  above  the  main  bed,  and  often  mined  separately  from 
it.  The  two  have  the  following  structure : 

Ft.  in. 

Coal 0 6^  Ft.  in. 

Slate- 0 4 > 2 8 

Coal 1 10  j 

Shales 12-20 

Coal 0 9 

Slate,  streak 0 0 

Coal 2 6 

Slate,  streak 0 0 


4 3 


. 

white.]  SECTION  IN  BELMONT  COUNTY,  OHIO  67 

Section  on  Federal  Creek , Ohio. — In  the  Federal  Creek  field  of  Athens 
and  Morgan  Counties,  Ohio,  the  coal  shows  as  follows  (Lovejoy),  op. 
cit.,  p.  648,  Heyburn  Brothers  & Co.’s  mine,  Berne  Township,  Athens 
County : 

/.  Ft.  in. 


Coal 1 10^ 

Slate,  streak 0 0 

Coal 2 4 

Slate 0 7 I Ft. 

Coal 0 3 > 10 

Clay 1 0 

Coal. 1 0 

Slate,  streak 0 0 

Coal 3 0, 


Section  at  Berry's  mine , Ohio. — Berry’s  mine,  in  Homer  Township, 
Morgan  County  (op.  cit.  page  650),  gives  the  following : 

Ft.  in. 


Coal : 0 11 

Slate,  streak 0 0 I 

Coal 3 5 f 5 4 

Clay 1 0 j 

Coal 0 4*1 

Slate,  streak * 0 0 

Coal 0 7\ 

Slate,  streak 0 0 ► 3 7* 

Coal 1 10 

Slate,  streak 0 0 

Coal 0 9f 

• 


The  clay  stratum  in  these  and  other  mines  appears  to  correspond  to 
the  main  clay  parting  which  always  separates  the  roof  coals  of  the 
Pittsburgh  bed  from  the  main  bench  along  the  Monongahela,  and  the 
12  to  20  feet  of  shales  which  separate  the  two  coal  beds  in  the  Shade 
Creek  field  would  appear  to  belong  at  the  same  horizon. 

East  from  the  barren  area  of  the  Pittsburgh  coal  of  Morgan,  Noble, 
and  Washington  Counties,  Ohio,  it  comes  in  again  with  a fine  develop- 
ment in  Belmont,  Harrison,  and  Jefferson. 

Section  in  Belmont  County , Ohio. — The  following  section  from  Ohio 
Geology,  Yol.  YI,  page  621,  exhibits  the  structure  in  the  southern  por- 
tion of  Belmont  County,  Washington  Township,  as  given  by  Prof. 
Brown : 


Ft. 

in.  Ft. 

iu. 

Coal 

° l 1 

Clay 

0 

10-12  ( 1 

11 

Coal 

2 

9 1 

Slate  

0 

01  | 

Coal 

2 

0 )>  6 

0 

Slate  

0 

oi| 

Coal 

1 

2 J 

68 


THE  NORTHERN  BITUMINOUS  COAL  FIELD. 


[BULL.  65. 


Section  at  Bellaire,  Belmont  County , Ohio. — In  Bellaire  the  following 
is  shown  at  Heatlierington’s  mine: 


Ft.  in. 
1 0 


I 

| Ft.  in. 
} 3 2 

J 


Coal 

Black  slate 0 4 

Coal •- 1 0 

Clay 0 10 

Coal 2 6 

Slate 0 0 

Coal 0 5 

Slate 0 0 

Coal 1 9 

Black  slate,  pyritous 0 01 

Coal 1 0 

Hard,  slaty  coal 0 4 

Section  in  Jefferson  County , Ohio . — In  Warren  Township,  Jefferson 
County,  Ohio,  this  coal  has  the  following  structure  (Brown,  Ohio  Geol- 
ogy, Vol.  VI,  page  603) : 


6 0* 


Roof  coal ' 

Clay 

Coal 

Clay  parting 

Coal 

Black  slate v 0 

Coal 1 

Parting 

Coal 1 


Ft. 

2 

0 

2 

0 

0 


3 

4 
2 
2 
2 
£ 

3 

2J 


Ft.  in. 
2 7 


> 4 11 


Section  in  Harrison  County , Ohio. — In  German  Township,  Harrison 
County,  Ohio,  Stevenson  reports  the  Pittsburgh  coal  as  follows  (Ohio 
Geological  Survey,  Vol.  Ill,  p.  212): 


Ft.  in. 

Roof  coal,  not  exposed 0 


Coal...- 
Parting . 

Coal 

Parting . 
Coal.... 
Parting . 
Coal 


0 

9 1 
Oil 

6 | Ft.  in. 
li}  4 9£ 
2 
0£ 

2 j 


Section  at  Columbia  mine , Westmoreland  County , Pennsylvania. — As  a 
typical  section  of  this  coal  on  the  Monongahela  River  with  reference  to 
the  structure  of  the  main  bench  and  roof,  we  may  take  that  found  at  the 
Columbia  mine,  near  Webster  and  361  miles  above  Pittsburgh,  as  given 
by  Mr.  J.  Sutton  Wall  (K4,  Pennsylvania  Geological  Survey*,  p.  50) : 

Ft  in. 

4 3 


Roof  coals,  in  seven  divisions 

Ft. 

3 

in. 

° l 

Over-clay 

0 

6 i 

“ Breast7’  coal 

3 

8 ' 

Parting 

0 

0J 

“Bearing  in”  coal 

0 

3 

Parting 

0 

0£  ► 

“ Brick  ” coal 

1 

2 

Parting 

0 

01 

“Bottom ” coal 

1 

4 J 

WHITE] 


FOSSILS  OF  THE  UPPER  COAL  MEASURES. 


69 


A careful  comparison  of  the  structure  of  this  famous  bed  at  a great 
many  points  very  widely  separated  exhibits  such  a striking  resemblance 
to  that  just  given  above  that  we  can  scarcely  attribute  it  to  chance, 
but  must  find  the  explanation  in  the  prevalence  of  nearly  uniform  con- 
ditions over  the  immense  area  covered  by  the  Pittsburgh  marsh. 

The  great  excellence  of  this  coal  for  steam  and  domestic  purposes, 
and  also  for  the  manufacture  of  gas  and  coke,  combine  to  render  it  the 
most  valuable  bed  of  coal  in  the  entire  Appalachian  field. 

Page  plate  6 gives  a view  of  this  bed  at  Conoellsville,  the  center  of 
the  coke-making  industry,  and  in  this  the  peculiar  columnar  structure 
of  a typical  coking  coal  is  fairly  shown. 

It  was  formerly  believed  that  this  bed  would  not  make  first-class 
coke  over  any  large  area  outside  of  the  Oonuellsville  basin,  but  recent 
developments  along  the  Monongahela  River  in  Marion  and  Monongalia 
Counties,  West  Virginia,  have  proved  this  belief  erroneous,  since  it  is 
there  successfully  coked  on  a large  scale. 

By  crushing  and  washing,  where  there  is  too  much  sulphur  present, 
there  is  no  reason  why  this  bed  will  not  make  coke  equal  to  that  of  the 
Connellsville,  throughout  all  of  the  region  south  and  west  from  the 
latter. 

The  roof  coals  of  this  bed  are  never  mined ; not  because  they  do  not 
furnish  good  fuel,  but  because  they  are  always  interstratified  with 
shale,  which  renders  the  mining  difficult.  These  roof  layers  often 
amount  to  3 or  4 feet  of  good  coal,  and  thus  this  large  quantity  of  fuel 
is  continually  wasted,  though  the  time  will  doubtless  come  in  the  dis- 
tant future  when  the  Pittsburgh  bed  will  be  mined  over  again  for  the 
coal  now  neglected  in  its  roof  and  bottom. 

FOSSILS  OF  THE  UPPER  COAL  MEASURES. 

The  flora  of  the  Pittsburgh  roof  shales  as  well  as  of  the  entire  Upper 
Coal  Measures  is  very  meager,  and  only  a few  of  the  very  common 
types,  like  Neuropteris  hirsuta , N.  flexuosa , and  Pecopteris  arborescent, 
are  usually  found,  while  the  fauna  of  the  whole  group,  so  far  as  known 
at  present,  seems  to  be  restricted  to  fresh  water  types. 


CHAPTER  IV. 


THE  BARREN  MEASURES,  OR  ELK  RIVER  SERIES. 

THICKNESS,  CHARACTER,  AND  EXTENT. 

Below  the  Pittsburgh  bed  we  descend  into  a very  natural  group  of 
rocks  (No.  XIV)  which  was  long  ago  clearly  recognized  by  the  Rogers 
brothers  in  both  Pennsylvania  and  Virginia.  The  group  as  defined  by 
them  extended  from  the  base  of  the  Pittsburgh  coal  down  to  the  top  of 
the  Mahoning  sandstone,  and  was  called  the  Lower  Barren  Measures ; 
but  subsequent  investigation  seems  to  render  it  more  desirable  to  ex- 
tend the  group  downward  so  «as  to  include  the  Mahoning  sandstone. 
This  brings  the  group  within  the  definite  limits  of  two  important  and 
very  persistent  coal  beds,  the  Pittsburgh  above  and  the  Upper  Free- 
port below;  and  hence,  for  purposes  of  comparison,  study,  and  all  the 
uses  which  classification  subserves,  is  more  desirable  than  the  old 
system,  since  the  top  of  the  Mahoning  sandstone  is  too  variable  a 
quantity  for  the  limit  of  any  group. 

I have  already  indicated  in  a previous  chapter  that  a larger  view  of 
the  Carboniferous  Measures,  which  overlooks  details  invaluable  for 
classification  to  the  working  geologist,  would  run  a line  through  the 
middle  of  the  Barren  Measures,  and  call  everything  above  it,  to  the 
top  of  the  Dunkard  Creek  series,  Upper  Carboniferous;  that  below  it, 
to  the  base  of  the  Pottsville  conglomerate,  Middle  Carboniferous,  and 
the  rest  down  to  the  Catskill,  Lower  Carboniferous.  Such  a classifica- 
tion of  the  Appalachian  Carboniferous  may  be  useful  for  comparison 
with  the  Carboniferous  system  in  other  regions  and  countries,  but  it  is 
too  general  for  the  practical  geologist,  and  can  never  supplant  that 
which  has  stood  the  test  of  long  and  continuous  use.  Hence  we  deem 
it  best  to  retain  the  limits  of  the  Barren  Measures  intact,  with  the 
slight  modification  just  suggested,  and  already  long  in  use  by  the 
Second  Geological  Survey  of  Pennsylvania. 

I have  adopted  the  name  Elk  River  series  as  a geographical  designa- 
tion for  these  beds,  since  they  are  very  finely  exposed  along  that  stream 
between  its  mouth  at  Charleston,  West  Virginia,  and  Braxton  Court- 
House,  or  Sutton,  nearly  100  miles  above. 

70 


WHITE.] 


THE  ELK  RIVER  SERIES. 


71 


This  series,  as  thus  limited  above  and  below  by  important  coal  beds, 
consists  of  two  very  different  members;  an  upper  one  composed  largely 
of  shales,  therefore  soft,  easily  eroded,  and  always  making  rounded 
hills  and  rolling  topography ; the  other,  or  lower,  composed  largely  of 
massive  sandstones  which  resist  erosion  and  thus  form  steep  cliffs,  deep 
gorges,  rugged  topography,  and  wild  scenery  generally. 

These  sand  rocks  form  a coping  to  the  Lower  Coal  Measure  hills,  and 
cap  the  summits  long  after  the  soft  beds  above  have  disappeared. 

The  soil  formed  by  the  soft  member,  while  rather  thin  and  not  to  be 
compared  in  fertility  to  that  of  the  Upper  Coal  Measures,  yet  with  care 
and  a liberal  use  of  lime  yields  excellent  crops  and  always  makes 
good  grazing  lands.  But  the  lower  portion,  being  almost  destitute  of 
lime,  and  containing  so  much  sand,  forms  a very  poor  soil,  on  which 
only  the  scantiest  crops  can  be  grown. 

The  upper  portion  always  contains  a large  percentage  of  red  and 
marly  shales,  which  make  a broad  band  of  red  soil  from  Pennsylvania 
clear  through  central  West  Virginia,  to  and  beyond  the  Kentucky  line 
on  the  one  hand,  and  thence  circling  around  through  eastern  Kentucky 
and  southern  Ohio,  back  to  Pennsylvania  again  on  the  other.  These  red 
clays  are  the  fruitful  source  of  landslides,  bad  roads,  and  many  other 
troubles.  They  cave  easily  in  drill  holes,  and  thus  give  endless  annoy- 
ance and  expense  to  oil  and  gas  drillers.  Their  tendency  to  slide 
causes  much  expense  in  cleaning  out  railroad  cuttings,  so  that  a proper 
knowledge  of  their  character  by  engineers  would  lead  to  economy  of 
money  in  building  and  maintaining  both  railroads  and  wagon  roads. 

The  coal  beds  of  this  series  are,  with  one  or  two  exceptions,  noted 
for  their  variableness  and  uncertainty.  They  may  be  in  fair  develop- 
ment on  one  farm,  and  absent  entirely  on  the  adjoining  one.  They  are 
also  usually  rich  in  ash  and  poor  in  carbon,  and  although  they  are 
patchy  in  their  distribution,  yet  the  main  beds  appear  to  maintain  the 
same  horizons  in  the  stratigraphy,  and  can  thus  be  identified  with 
reasonable  certainty  over  wide  areas.  The  sandstones  found  within 
the  limits  of  this  group  are  of  more  economic  importance  than  the  coal 
beds,  since  the  former  nearly  always  furnish  most  excellent  building 
stone,  while  the  latter  are  commercially  valuable  only  over  limited 
areas.  Iron  ore  in  valuable  quantity  exists  locally  at  several  horizons 
in  the  Barrens,  and  these  will  be  referred  to  hereafter  in  detail. 

The  limestones  of  this  series,  like  the  coals,  are  generally  thin  and 
impure,  so  that  they  are  of  more  importance  in  determining  the  strati- 
graphy than  for  economic  purposes. 

The  entire  thickness  of  the  group  varies  much  in  different  portions 
of  the  Appalachian  field,  reaching  a maximum  of  800  feet  in  the  vicinity 
of  Charleston,  West  Virginia,  while  along  the  northwestern  outcrop  of 
the  beds  in  Ohio  the  minimum  is  not  much  above  300  feet. 

In  Pennsylvania  and  northern  West  Virginia  the  average  is  about 
600  feet,  but  it  sometimes  runs  up  to  650  and  down  to  550. 


72 


THE  NORTHERN  BITUMINOUS  COAL  FIELD. 


[BUM..  65. 


The  following  sections,  taken  in  the  several  portions  of  the  Appa- 
lachian held,  will  serve  to  illustrate  both  the  changing  thickness  of  the 
series  and  the  variable  nature  of  the  individual  beds. 

Section  in  the  Pittsburgh  region. — We  shall  begin  the 
list  at  Pittsburgh,  where  the  upper  half  of  the  Bar- 
rens is  finely  exposed,  and  the  numerous  carefully 
kept  records  of  drill  holes  have  revealed  the  constitu- 
tion of  the  lower  half,  so  that  by  uniting  the  two  we 
get  the  following  (Fig.  33) : 


7t>* 


ilil 


iSi 


mm 


In  Pittsburgh  region. 


[See  map,  I m.] 


Pittsburgh  coal 

Concealed 

Limestone 

Shales,  variegated 

Limestone 

Rod  shale 

Concealed 

Sandstone,  Morgantown 

Coal,  Elk  Lick 

Shales,  variegated 

Coal 

Limestone 

Shales,  variegated 

Limestone,  crinoidal * 

Coal,  crinoidal 

Red  and  variegated  shale 

Sandy  shales  and  shaly  sandstone 

, Coal,  Bakerstown 

Shales  and  sandstone 

Limestone,  Upper  Cambridge 

Sandstone,  massive 

Limestone,  Lower  Cambridge 

Shales 

Coal,  Masontown 

Shales 

Sandstone,  Mahoning 

Upper  Freeport  coal. 

Total 


Ft. 


Ft. 


227 


90 


114 


2 

50 

1 

10 

1 

20 

100 


618 


Fio.  33.— Section  in 
the  Pittsburgh  region. 


WHITE.  ] 


THE  BARREN  MEASURES. 


73 


Section  at  Sewickley , Pennsylvania.— At  Sewickley,  Pennsylvania,  a 
diamond-drill  hole  was  put  down  by  Mr.  Cochran  Fleming  as  a test 
for  coal.  The  cores  were  carefully  preserved,  and 
from  them  I obtained  a very  accurate  section  of  t lie 
lower  portion  of  the  Barrens,  which,  combined  with 
the  good  surface  exposures  around  Sewickley,  gives 
the  following  structure  (Fig.  34)  for  this  series  in 
that  region : 


205* 


■I 


ao' 


4 tf 


WMm  38'5" 

ivXvXvV’/. 


I35’> 


Sewickley,  Alleghany  County,  Pennsylvania. 

[See  map,  HI.] 

Ft.  in. 

1.  Pittsburgh  coal 

2.  Shales,  sandstones,  and  concealed 180 

3.  Sandstone,  Morgantown,  massive 25 

4.  Coal,  Elk  Lick  

5.  Shales  and  sandstone 

6.  Limestone,  crinoidal 

7.  Coal,  crinoidal 1 

8.  Red  shales  and  sandy  beds 110 

9.  Limestone,  gray,  Upper  Cambridge 2 

10.  Shales  and  concealed 40 

11.  Sandy  shale 32 

12.  Dark  slate 11 

13.  Limestone,  dark,  Lower  Cambridge 

14.  Dark  shales 

15.  Coal,  Mason  town 

16.  Sandstone,  micaceous,  gray 13 

17.  Fire  clay,  sandy 0 

18.  Sandstone,  light  gray 22 

19.  Shale,  dark  gray 8 

20.  Sandstone,  gray 0 

21.  Shale,  sandy 6 

22.  Shale,  blue 6 

23.  Sandstone 0 

24.  Slate,  gray 3 

25.  Fire  clay,  variegated  at  base,  impure 25 

26.  Sandstone,  gray,  micaceous 38 

27.  Shales,  sandy,  blue 8 

28.  Sandstone,  light  gray 8 

[ 29.  Upper  Freeport  coal. 


Total . 


Ft. 


205 


6 ) 


196 


. 135  7 

sy*  ' 


634 


Fig.  34. — Section  at 
Sewickley,  Pa. 


The  interval  No.  2 in  this  section  was  estimated, 
since  the  Pittsburgh  coal  is  not  found  in  the  imme- 
diate vicinity  of  Sewickley,  the  highest  stratum 
remaining  there  being  the  Morgantown  sandstone, 
No.  3. 


74 


THE  NORTHERN  BITUMINOUS  COAL  FIELD. 


[BULL.  65. 


Section  on  Dunbar  Creek , Pennsylvania. — Eastward  from  the  Pittsburgh 
region,  we  have  a line  of  measurements  of  the  Barren  series  which  ex- 
tend across  the  Alleghanies.  The  first  one  is  in  the 
adjoining  county  of  Fayette,  at  the  foot  of  Chest- 
nut Bidge,  made  by  Prof.  Stevenson  and  published 
in  his  Beport  KK,  page  182.  It  is  as  follows  (Fig. 
35): 

Dunbar  Creek , Fayette  County , Pennsylvania. 


42' 


65* 


35' 


[See  map,  K n.] 


Fig.  35.— Section  on 
Dunbar  Creek,  Pa. 


1.  Coal,  Pittsburgh 

2.  Concealed... , 15 

3.  Sandstone 10 

4.  Coal,  Little  Pittsburgh  0 

5.  Clay 3 

6.  Limestone  and  shale 20 

7.  Sandstone,  Connellsville 60 

8.  Shales 50 

9.  Limestone.! 5 

10.  Shale 5 

11.  Sandstone,  Morgantown 55 

12.  Shale,  sandy* 12 

13.  Coal,  Elk  Lick 

14.  Shale 12 

15.  Concealed 12 

16.  Shale,  variegated 35 

17.  Coal,  clay,  crinoidal 

18.  Shales,  brown 10 

19.  Sandstone 28 

20.  Shale J 45 

21.  Coal,  Bakerstown 2 

22.  Shale 63 

23.  Limestone,  Lower  Cambridge 

24.  Shale 7 

25.  Sandstone,  argillaceous 10 

26.  Concealed 25 

27.  Coal,  Masontown 

28.  Clay 30 

29.  Sandstone,  Upper  Mahoning 35 

30.  Coal,  Mahoning 

31.  Fire  clay 

32.  Sandstone,  Lower  Mahoning 

33.  Coal,  Upper ‘Freeport. 

Total 


Ft.  in.  Ft.  m. 


235 


148 


598  6 


The  identification  of  the  Lower  Cambridge  limestone  in  the  above 
section  is  open  to  question,  but  the  probabilities  are  in  favor  of  the  one 
given. 


WHITE.] 


THE  BARREN  MEASURES, 


75 


Section  at  Ligonier , Pennsylvania. — Eastward  from  the  last  locality, 
and  between  Chestnut  Ridge  and  Laurel  Hill,  the  following  section 
(Fig.  36)  of  these  beds  was  measured  at  Ligonier, 
Westmoreland  County,  Pennsylvania,  by  Prof.  Stev- 
enson, as  given  in  Report  KKK,  page  129 : 


Ligonier , Westmoreland  County,  Pennsylvania . 


L===s§r==2o 


153? 


[See  map,  J p.] 

Ft.  in. 

1.  Pittsburgh  coal 

2.  Concealed 60 

3.  Coal,  Little  Pittsburgh 1 6 

4.  Limestone 8 

5.  Concealed 27 

6.  Shale,  variegated 43 

7.  Coal,  Little  Clarksburg . 

8.  Shale 10 

9.  Concealed 10 

10.  Sandstone,  Morgantown 115 

11.  Shale,  olive  .* 18 

12.  Coal,  Elk  Lick 

13.  Shale 

14.  Limestone,  green,  fossiliferous 

15.  Shale 20 

16.  Sandstone 5 

17.  Clay 8 

18.  Limestone,  ferruginous 2 

19.  Shale 10 

20.  Sandstone 25 

21.  Concealed 100 

22.  Shale 5 

23.  Sandstone,  Upper  Mahoning 

24.  Shale 

25.  Coal,  blossom,  Mahoning 

26.  Concealed 50 

27.  Sandstone,  Lower  Mahoning 25 

28.  Shale 5 

29.  Coal,  Upper  Freeport. 


Total . 


Ft.  in. 


} 139  6 


153 


j>  175 


80 


602 


Fig.  36.  — Section  at 
Ligonier,  Pa. 


This  and  the  preceding  section,  as  well  as  the  one 
which  follows,  illustrate  in  a remarkable  manner  the 
rapid  variation  in  the  individual  elements  of  the  Barrens,  while  the 
total  thickness  remains  almost  exactly  the  same. 


76 


THE  NORTHERN  BITUMINOUS  COAL  FIELD. 


[bull.  65. 


Section  near  Berlin , Pennsylvania.— Still  farther  east,  in  the  Berliu 
basin  of  Somerset  County,  Pennsylvania,  and  on  the  very  summit  of 
the  Alleghany  Mountains,  we  find  this  series  with  the  following  struc- 
ture (Fig.  37)  as  determined  byr  Messrs.  Platt,  with  some  additions  and 
modifications  by  the  writer : 


l^S"6" 


•6  2V 
' i 
15’ 


446,' 


Fig.  37.— Section 
near  Berlin,  Pa. 


Vicinity  of  Berlin,  Somerset  County , Pennsylvania. 


[See  map,  K p.] 


Ft.  in.  Ft.  in. 


' 2") 
' 4"\ 
' 6'0 

1'  8") 
0'  8"  > 
V 4"  > 


1.  Pittsburgh  coal 

2.  Interval,  shales,  sandstones,  etc 

3.  Coal 

4.  Limestone,  gray  and  buff 10 

5.  Concealed 50 

6.  Sandstone,  massive 25 

7.  Shales,  dark 15 

f Cannel  slate 1'  1 

8.  Coal,  Platt  (crinoidal) . . j§^slaty j- 

9.  Sandy  shales  and  black  slates 50 

t Coal 3'  2" 

10.  Coal,  Price  (’Bakersto'wn)  < Slate O' 

f Coal O' 

11.  Slates,  dark 4 

f Limestone..  1'  8"; 

12.  Limestone,  dark  gray . . < Slate 

( Limestone . 

13.  Shale 0 

14.  Coal 1 

15.  Shales,  and  concealed 45 

16.  Coal,  Coleman 1 

17.  Slate,  dark 0 

18.  Limestone,  Coleman  (Upper  Cambridge) 

19.  Shales 10 

20.  Sandstone,  and  concealed 15 

21.  Shales,  sandy 15 

( Coal V 3"1 

22.  Coal,  Philson < Slate,  black 0'  9"  > 2 

(Coal O'  6") 


23.  Fireclay 2 

24.  Limestone,  Philaoo  5 ‘ ' V 2"'. 

(Lower  Cambridge)}  Stalest  *,  s 


25.  Concealed,  and  shales 25 

26.  Coal,  Masontown 2 

27.  Concealed 5 

28.  Sandstone,  Mahoning,  and  concealed 100 

29.  Coal,  Upper  Freeport. 

Total 


200 

1 

] 

s 100 


;•  no  4 


44  6 


132 


599 


Section  at  Broad  Top , Pennsylvania. — As  showing  the  remarkable 
persistence  of  this  series  in  its  general  thickness  over  the  Pennsylvania 


WHITE.  J 


THE  BARREN  MEASURES. 


77 


field,  we  give  another  measurement  (Fig.  38)  from  far  east  of  the 

Alleghany  Mountains,  in  the  center  of  the  Broad  Top 

Basin,  Bedford  County,  Report  T2,  Stevenson,  page  60 : 

n 


Broad  Top,  Bedford  County,  Pennsylvania. 


[See  map,  J t.]  Ft. 

1.  Pittsburgh  coal 

2.  Poorly  exposed  (shales  and  sandstones) 425 

3.  Sandstone,  Upper  Mahoning 50 

4.  Coal,  Mahoning 5 

5.  Clay 3 

6.  Sandstone,  Lower  Mahoning 40 

7.  Coal,  Upper  Freeport. 


Total. 


523 


Fig.  38. — Section 
at  Broad  Top, 
Pa. 


Section  opposite  Steubenville , Ohio. — The  next  line  of 
sections  in  this  series  across  the  Appa- 
lachian field  will  begin  at  Steubenville,  on 
the  Ohio  River,  and  keeping  south  of  the 
former  line,  end  at  Davis,  Tucker  County, 

West  Yirginia.  The  following  succession 
(Fig.  39)  was  obtained  opposite  Steuben- 
ville by  combining  the  surface  observa- 
tions with  the  records  of  drill  holes  and 
shafts : 


Opposite  Steubenville,  Ohio. 

[See  map,  Ij.] 

1.  Pittsburgh  coal 

2.  Shales,  sandstone,  and  concealed 100 

3.  Shales 

4.  Sandstone,  massive,  Morgantown 

5.  Limestone,  fossiliferous,  crinoidal 

6.  Red  shales 

7.  Concealed,  with  shales  and  flaggy  sand- 

stone   < 

8.  Coal 

9.  Shale 

10.  Limestone,  fossiliferous,  Lower  Cam- 

bridge   

11.  Shales,  drab 

12.  Shales,  with  coal,  Masontown 

13.  Shales,  gray  

14.  Sandstone,  Mahoning,  and  concealed 

under  river  130  J 

15.  Coal,  Upper  Freeport. 

Total 


Ft. 

Ft. 

100  ' 

) 

15 

> 200 

85  J 

) 

10 

40  ] 

I 

100 

!>  142 

1 I 

1 J 

1 

8 1 

2 

5 

J-  145 

130  J 

499 


This  shows  a westward  thinning  of  about  100  feet 
for  the  series  between  Pittsburgh  and  Steubenville. 

Section  under  Washington , Pennsylvania. — Near  Wash- 
ington, Pennsylvania,  many  wells  drilled  for  gas  and 
oil  have  revealed  the  structure  of  the  Barren  Measures, 
although  they  lie  many  hundred  feet  below  the  surface. 

One  of  these  borings  was  supervised  by  Prof.  Lin- 
ton, of  Washington  and  Jefferson  College,  and  from 
the  record  thus  obtained  of  the  Thayer  oil  well,  as 


85' 


200' 


mm 


v.v! 

~-Vv 


!. 


m 


1 42' 


l30’M45r 


Fig.  39. — Section 
opposite  Steuben- 
ville, Ohio. 


78 


THE  NORTHERN  BITUMINOUS  COAL  FIELD, 


1 1 BULL.  65. 


published  in  Pennsylvania  Geological  Beport,  1886,  page  764,  we  get 
the  following  for  the  Barrens  there  (Fig.  40) : 

Washington,  Pennsylvania . 


1. 

2. 

3. 

4. 

5. 

6. 

7. 

■220*  8. 
9. 
10. 
11. 
12. 

13. 

14. 

15. 

16. 


60' 


20' 


183 


32f 


2sr 


[See  map,  J k.] 


Ft. 


Coal,  Pittsburgh 

Sandstone 

Shale,  black  and  red 

Shale,  red 

Limestone 

Sandstone,  Morgantown 

Shale,  black  25] 

Shale,  red  and  variegated 

Sandstone,  hard 

Shale,  black 

Sandstone  

Shale,  red.  variegated 

Sandstone,  Upper  Mahoning 

Shale,  olive  green  

Sandstone,  Lower  ( gray,  fineflaggy  ..15' 

Mahoning. < white 17' 

Shale,  dark,  to  place  for  Upper  I-  reeport 
coal 


65] 
70  | 
30  > 
5| 
50  j 


20  l 
37  f 
17  | 
34  J 


Ft. 


220 


193 


28 


Near  Cannonshurg,  Washington  County,  Penn 
sylvania. 

[See  map,  Jl.J  Ft. 

1.  Coal,  Pittsburgh 

2.  Limestone,  blue,  hard 

3.  Slate,  white,  soft 

4.  Shale,  red 

5.  Slate,  black 

6.  Shale,  red 

7.  Sandstone,  gray,  hard 

8.  Slate,  black  

9.  Sandstone,  gray,  hard,  Morgantown 


20] 
45  I 
36  | 

47  f 

IS  I 

38  J 


Ft. 


225 


Fig.  40.— Section  at 
Washington,  Pa. 


10.  Shale,  red 25  ] 


11.  Slate,  black 

12.  Sandstone,  gray,  hard 

13.  Slate,  white,  soft 

14.  Sandstone,  gray,  hard — 

15.  Slate,  black 

16.  Sandstone,  gray,  hard 

17.  Slate,  black 

18.  Sandstone,  gray,  hard 

19.  Slate,  black 


5 

20 
10 
20 
15 
10 
25 
5 
10 

20.  Sandstone,  gray,  hard 20 


21.  Shells  and  slate,  gray,  hard. 

22.  Slate,  black,  soft 

23.  Slate,  with  coal,  Mahoning 

24.  Shells,  gray,  hard 

25.  Slate,  black,  soft  

26.  Sandstone,  white,  hard,  Lower  Mahoning. 

27.  Coal.  Upper  Freeport. 


25  J 


Total . 


190 


557 


Total 548 

Nos.  8 and  12  are  the  beds  which 
“cave”  and  give  the  oil  drillers  so  much 
trouble. 

Section  near  Gannonsburg , Pennsylva- 
nia.— In  the  vicinity  of  Cannonsburg,  a 
few  miles  northeast  from  Washington, 
the  record  of  a well  drilled  for  gas  on  the 
Boyce  farm,  furnished  me  by  Mr.  Wm. 
S.  Stevenson,  assistant  superintendent  of 
the  Philadelphia  Natural  Gas  Company, 
gives  the  following  (Fig.  41)  as  the  struc- 
ture of  the  Barrens  there  : 


40* 


Fig.  41.— Section 
near  C anno  n s- 
burg,  Pa. 


WHITE.’ 


THE  BARREN  MEASURES. 


79 


Section  at  Morgantown , West  Virginia. — From  Washington  across  to 
Morgantown,  West  Virginia,  the  Barren  Measures,  as  revealed  by  bor- 
ings, hold  about  the  same  thickness  as  in  Washing- 
ton County.  In  the  vicinity  of  Morgantown  the 
entire  column  of  the  Barrens  is  exposed,  and  there 
the  following  structure  is  exhibited  (Fig.  42) : 


20 


227tf' 


S5'6* 


00 


4o' 


LS 7'C 


Morgantoivn,  Monongalia  County , West  Virginia . 

[See  map,  Mm.] 


1.  Pittsburgh  coal  

2.  Fire  clay 

3.  Sandy  shales  and  sandstone 

4.  Coal,  Little  Pittsburgh 

5.  Sandy  shales 

6.  Limestone 

7.  Yellowish  shales  with  iron  ore 

8.  Sandy  shales,  and  concealed 

9.  Sandstone,  rather  massive 

10.  Sandy  shales,  and  concealed 

11.  Massive  sandstone 

12.  Bluish  green  sandy  beds 

13.  Black  slate,  fossiliferous 

14.  Limestone,  Clarksburg 

15.  Shales  and  sandy  beds 

16.  Sandstone,  Morgantown 

17.  Elk  Lick  coal 

18.  Shales,  and  concealed 

19.  Limestone,  crinoidal 

20.  Variegated  shales 

21.  Limestone,  Upper  Cambridge 

22.  Shales.. 

23.  Sandstone,  Upper  Mahoning 

24.  Shales  and  slialy  sandstone. . . r 

25.  Massive  sandstone,  Lower  Mahoning. 

26.  Shales 

27.  Coal,  Upper  Freeport. 

Total 


227 


Ft.  in.  Ft.  in. 

2 1 
32 
1 

17 
1 

10 
17 
25 
15 
20 
20 
1 
1 
45 
20 

3 
55 

1 

85 

1 

14  ! 

3 6 | 

30 
100 
40 


187 


561 


The  black  fossiliferous  slate,  No.  13,  represents 
fig.  42.— section  at  Mor-  the  horizon  of  the  Little  Clarksburg  coal,  and  is 
here  filled  with  fish  teeth  and  scales.  The  Ujpper 
Freeport  coal  is  about  100  feet  under  the  river  at  the  Morgantown 
wharf,  but  southward  it  rises  very  rapidly  and  comes  up  to  the  bed  of 
the  river  at  the  mouth  of  Coburn’s  Creek,  2 miles  above.  It  is  there 
about  4 feet  thick  and  very  pure. 


80 


THE  NORTHERN  BITUMINOUS  COAL  FIELD. 


[bull.  65. 


Section  near  Little  Falls , West  Virginia . — In  the  vicinity  of  Little 
Falls,  Monongalia  County,  9 miles  above  Morgantown,  the  basal  mem- 
bers of  the  Barrens  can  be  obtained  more  in  detail 
than  in  the  Morgantown  section,  and  the  following 
(Fig.  43)  shows  the  structure  there : 

Little  Falls,  Monongalia  County , West  Virginia. 

, * [See  map, 


m.] 


47' 


a*.' 


=.==24,6" 


s- iz'  >9a'a' 


Z6'6" 


Fig.  *43. — Section  at  Lit- 
tle Falls,  W.  Va. 


1.  Pittsburgh  coal 

2.  Shales,  sandstones,  and  concealed . . . 

3.  Sandstone,  in  knob 

4.  Shales 

5.  Massive,  coarse  yellow  sandstone  — 

6.  Coaly  shale,  Little  Clarksburg 

7.  Limestone,  fossiliferous,  Clarksburg 

8.  Concealed,  shales  and  sandstone 

9.  Limestone,  nodular 

10.  Gray  and  yellow  shales 


Ft.  in.  Ft.  in. 

) 


100 

5 

15 

21 

0 

1 

47 

3 


.macK  siate 

I 

f ( Coal 

...  12")  ) 

j Coal . < Slate 

...  1">  V 5" 

Coal,  Elk  Lick  . { 

t Coal 

. . . 4" S S 

Concealed  with  red  shale.  15' 

• i 

' Coal,  good 

O'  6"  j 

13.  Shales 

14.  Limestone,  gray  and  buff  in  several  layers,  Elk  Lick. 

15.  Flaggy  sandstones  and  shales 

16.  Sandstone,  massive,  pebbly  at  base  for  4 feet 

17.  Concealed,  probably  shales , 

18.  Fossiliferous  shale,  crinoidal 

19.  Concealed,  red  shales  and  impure  limestones 

20.  Limestone,  light  gray,  TJpper  Cambridge 

21.  Shales  and  flaggy  sandstones 

22.  Sandstone,  rather  massive 

23.  Concealed,  and  shales 

24.  Sandstone,  Upper  Mahoning,  massive 

25.  Coal,  Mahoning 

26.  Shales  and  concealed 

27.  Shale,  greenish,  sandy , 

28.  Sandy  shale  and  flaggy  sandstone 

29.  Shale,  greenish  yellow 

30.  Concealed,  probably  shale 

31.  Lower  Mahoning  sandstone 

32.  Coal,  Upper  Freeport. 

Total 


205  9 


6 

22  10 

15 

31 


24  6 

10  10 


16  11 


83  4 


10 

65  6 

1 


16  3 f 106  1 

53  6 j 


27  1 

11 

5 2 I 

12 
17 

26  o j 


98  8 


587  3 


This  section  illustrates  well  the  variability  of  the  Barren  Measures, 
when  compared  with  the  previous  one,  taken  only  a few  miles  distant. 


WHITE.] 


THE  BARKEN  MEASURES. 


81 


Section  at  Newburg , West  Virginia. — The  syncline  between  the  Chest- 
nut Ridge  and  Laurel  Hill  anticlines  crosses  the  Baltimore  and  Ohio 
Railroad  at  Newburg,  Preston  County,  West  Virginia, 
about  15  miles  east  from  Little  Falls,  and  there  the 
Barren  Measures  admit  of  vertical  measurement  by 
combining  surface  exposures  with  the  record  of  the 
Orrel  Coal  Company’s  shaft.  The  result  is  as  follows 
(Fig.  44) : 


2J0 


Newburg,  Preston  County,  West  Virginia . 

[See  map,  N m.] 


iS' 


r 

20' 

5‘ 

4o 

to' 

1$’ 

20' 
10 f 
10' 

I o' 

J5’ 


95 


aor 


61) 
u a 
ga 
g ° 
©.a 

^3 


1. 
2. 

3. 

4. 

5. 

6. 

7. 

8. 

9. 

10. 
11. 
12. 

13. 

14. 

15. 

16. 

17. 

18. 
19. 

3 ] 20. 

l|21- 

P 122. 

23. 

24. 

25. 

26. 
27. 


fci  ( 
"a 


Pittsburgh  coal 

Fire  clay 

Concealed 

Shales,  sandy 

Concealed 

Sandstone,  pebbly,  Morgantown 

Concealed 

Sandstone,  flaggy 

Shales,  sandy 

Shales,  dark,  fossiliferous  (crinoidal) 

Concealed 

Red,  marly  shale  

Concealed 

Sandstone,  yellow 

Concealed - 

Fire  clay  and  shales 

Sandstone,  massive 

Sandy  shale 

Sandstone,  massive 

Concealed 

Sandstone 

Shales 

Coal,  Mahoning 

Sandstone — 

Shale 


28. 


Sandstone 

Shale 

Sandstone 

Coal,  Upper  Freeport. 


Ft. 

5 ) 

14  I 

30  > 
230  j 
30  J 

15  1 

1S[ 

10  J 

20 

5 

40 

10  \ 
15 

5 ) 
20  ) 
10 
10 
10  f 

35  I 
25  J 


34  > 
1 | 
3 J 


Total . 


80 


Ft. 


•309 


35 


15 


95 


no 


80 


645 


This  is  in  the  same  geological  trough  as  the  section 
at  Ligonier  (Fig.  36),  and,  as  will  be  observed,  agrees 
FlNewbm-g6w°vaat  ^ *n  having  an  unusually  large  interval  between 

the  Pittsburgh  coal  and  the  base  of  the  Morgantown 
sandstone.  It  is  possible  that  the  Upper  Mahoning  sandstone  should 
not  include  Nos.  17-20  at  thjs  locality. 

Bull.  65 6 


82 


THE  NORTHERN  BITUMINOUS  COAL  FIELD. 


[BULL.  65. 


Section  near  Fairfax  Knob , West  Virginia.— About  50  miles  east 
from  Newburg  we  come  to  the  North  Potomac  Coal  Basin,  the  south- 
ward extension  of  the  Cumberland  or  Georges  Creek 
field  of  Maryland,  and  there,  in  the  vicinity  of  Fairfax 
Knob,  Tucker  County,  West  Virginia,  the  Barrens  ex- 
& hibit  the  following  structure  (Fig.  45) : 

Fairfax  Knob,  Tucker  County,  West  Virginia. 

[See  map,  O o.] 


Ft. 


1.  Pittsburgh,  coal 

2.  Shales  and  concealed 


Ft.  in s 


85 


( Coal  2'  9"  ■ 
3 Coal,  Little  Pittsburgh  . . < Slate  . 0'  6"  ( 
(Coal..  O'  6" . 


4.  Shales 


5.  Coal 


f Coal,  slaty.  0'  10”  1 

j Coal  1'  5"  1 

i Slate V 0”  ( * 

I Coal V 0”J  • 


6.  Fire  clay  and  shalgs 

7.  Blue  shales  with  iron  ore 

8.  Black  slate 


C Coal..  O'  8”} 

9.  Coal,  Little  Clarksburg  . . < Slate  . O'  4”  V 

(Coal.  1' 0”  ) 

10.  Concealed,  with  sandstones  and  shales 

11.  Coal,  and  black  slate,  Masontown 

12.  Shales 

f 13.  Sandstone,  massive 

! 14.  Concealed ® 

l 15.  Sandstone,  soft 1 


y . 

^ ^ I 16.  Clay,  yellow 


[ 17.  Sandstone 

18.  Limestone,  Mahoning . 
Soft  shale 


u fl9' 

•g  20.  Hard  shale 


21.  Soft  shale 

^ s,  22.  Slate,  light  blue. 
23.  Slate,  dark 


[24.  Sandstone 

25.  Coal,  Upper  Freeport. 


20 

1 

9 

1 

10 

19 

2 


Total 


40 


200 

3 

50 


61 


20 


42 


538 


Fig.  45. — Section  at 
Fairfax  knob,  W. 

Va. 

The  last  100  feet  of  the  section  was  obtained  from  the  record  of  a 
diamond  drill  hole  put  down  by  the  West  Virginia  Central  Railroad 
to  test  the  character  of  the  Upper  Freeport  coal.  The  writer  saw  sam 
pies  of  the  Mahoning  limestone,  taken  from  the  drill  hole,  and  it  was 

a dark  gray,  rather  pure  limestone. 

No.  5 is  a second  Little  Pittsburgh  coal  which  is  occasionally  present 
in  the  Potomac  basin  and  elsewhere. 


WHITE.] 


THE  BARKEN  MEASURES. 


83 


Section  in  Guernsey  County , Ohio. — Toward  the  northwestern  side  of 
the  Appalachian  basin,  in  Ohio,  the  Barrens  are  thinner  than  elsewhere, 
as  may  be  seen  from  the  following  section  (Fig.  46), 
made  by  Mr.  F.  W.  Minshall,  in  Guernsey  County, 
Ohio. 


(Guernsey  County , Ohio. 

[See  map,  Kf.] 

Ft.  in. 

1.  Pittsburgh  coal 

2.  Shales 10 

3.  Limestone 15 

4.  Shales 30 

5.  Concealed 75 

6.  Shales 20 

7.  Limestone,  crinoidal 

8.  Coal,  crinoidal 1 3 


Ft.  in. 


> 150 

| 


9.  Shales 15 


mb'?  10.  Limestone 


10 


11.  Shales 35 

12.  Sandstone,  pebbly . 25 

13.  Shales 5 

14.  Coal,  Bakerstown 2 

15.  Shales 35 

16.  Limestone,  Lower  Cambridge. . 

17.  Shales -. 5 

18.  Coal,  Masontown 1 

19.  Shales 30 

20.  Sandstone,  Upper  Mahoning. . . 35 

21.  Coal,  Mahoning 1 

22.  Shales 5 

23.  Sandstone,  Lower  Mahoning. . . 30 

24.  Shales 5 

25.  Coal,  Upper  Freeport. 

Total 


> 112  11 


395  2 


Fig.  46. — Section  in 
Guernsey  County, 
Ohio. 


Section  at  Burning  Springs , West  Virginia. — At  Burn- 
ing Springs,  Wirt  County,  West  Virginia,  the  Barren 
Measures  have  the  following  structure  (Fig.  47),  ac- 
cording to  Mr.  Minshall: 

Burning  Springs , Wirt  County , West  Virginia. 

[See  map,  P g.] 

Ft.  in.  Ft.  in. 

1.  Pittsburgh  coal 

2.  Shales 10  ] 

3.  Limestone 10  j>  200 

4.  Concealed 180  j 

5.  Limestone,  crinoidal 3 

6.  Coal,  crinoidal 1 8 ) 

7.  Shales  10 

8.  Limestone 3 ! 

9.  Concealed  200  / 294  8 

10.  Sandstone  40 

11.  Shales 40  | 

12.  Coal,  Upper  Freeport. 

Total 407  8 


Fig.  47. — Section  at 
Burning  Springs,  W. 
Va. 


84 


THE  NORTHERN  BITUMINOUS  COAL  FIELD. 


[BULL.  65. 


Section  near  Huntington , West  Virginia. — Near  the  southwestern 
limit  of  the  district,  in  the  vicinity  of  Huntington, West  Virginia,  the 
Barren  Measures  have  the  following  structure  (Fig. 
48)  according  to  the  determinations  of  Mr.  A.  G. 
Selby,  who  made  careful  measurements  of  the  rocks 
exposed  there,  and  combined  them  with  the  record 
of  a boring  for  gas  : 


■Rl 


197' 


185* 


Vicinity  of  Huntington , West  Virginia , along  Ohio  River. 


[See  map,  S b.] 


1.  Pittsburgh  coal 

2.  Red  shale,  contaiuing  limestone  nodules 

3.  Sandstone,  skaly 

4.  Red  shales  and  shalv  sandstone 

5.  Coal,  Little  Clarksburg 

6.  Sandstone,  massive,  Morgantown 

7.  Elk  Lick  coal 

8.  Fireclay 

9.  Shales,  deep  red 

10.  Limestone,  crihoidal 

11.  Coal,  crinoidal 

12.  Red  shales 

13.  Limestone 

14.  Shales  and  sandstones 

15.  Limestone,  Lower  Cambridge 

16.  Shales 

17.  Coal,  Masontown 

18.  Shales 

19.  Sandstone,  Mahoning  

20.  Upper  Freeport  coal. 

Total 


Ft. 

28 

16 

101 

2 

50 

3 

103 

2 

4 
4 

175 

10 

1 

30 

125 


Ft. 

197 

2 

106 

2 

185 

2 

166 


Fig.  48.— Section  near 
Huntington,  W.Va. 


This  is  nearly  twice  the  thickness  that  the  Ohio 
geologists  report  for  the  Barrens  along  the  north- 
western margin  of  their  outcrop,  but  all  of  the  meas- 
ures thicken  very  rapidly  toward  the  southeast  from 
this  portion  of  Ohio.  It  is  possible,  however,  that 
Mr.  Selby  may  have  gotten  some  of  the  elements  of 
the  section  too  thick,  since  there  is  no  single  point 
between  Huntington  and  the  Big  Sandy  where  a ver- 
tical measurement  of  all  the  members  can  be  made. 
The  true  thickness  can  not  be  much  under  600  feet  at 
least. 


WHITE.] 


THE  BARREN  MEASURES. 


85 


Section  near  Charleston , West  Virginia. — In  the  vicinity  of  Charleston, 
West  Virginia,  and  just  north  from  it,  the  Barren  Measures  attain  a 
greater  thickness  than  anywhere  else  in  the  Appala- 
chian Basin,  so  far  as  known.  The  following  structure 
(Fig.  49)  may  be  observed  along  the  Great  Kanawha 
Kiver  there,  and  its  tributary,  Two- mile  Creek : 


Near  Charleston,  West  Virginia. 

fSee  map,  S f.] 


Ft. 

Pittsburgh  coal - 

Concealed  red  shales  and  sandstone.-. 140 

Sandstone,  massive 30 

Red  shales,  sandstone  and  concealed 150 

Coal,  Elk  Lick 

Shales 

Sandstone 

Shales,  marly,  with  limestone  nodules 

Limestone,  impure  (crinoidal  horizon) 

Dark  red  shales  with  iron  nodules 

Shales 

Coal,  impure,  Bakerstown 

Eire  clay  and  shales 

Sandstone,  massive,  pebbly 

Shales  and  sandstone 

Shales,  with  streaks  of  coal,  Masontown 

Sandstone,  very  hard ,-••?- ■ 

Coal,  Mahoning  . . . .4.  F.  . . .* 

Massive  sandstone 

Shales 

Coal,  Upper  Canneltonr. . .( .4r.  F>. . 

Sandstone,  massive. 

Sandy  shales , 

Coal,  Middle  Cannelton >.  K . .'A Jl 

Black  flint 1 

Shales .. 

Coal,  Upper  Freeport. 


10 

30 

30 

30 

25 

5 

5 

30 

100 

20 

25 

4 

75 

10 

2 

50 

15 

1 

5 
2 


Ft. 

320 

1 

70 

5 

► 215 

1 


Total . 


800 


7 s’ 

iliil 

vS 

so* 

m 

15' 

V j 

Fig.  49.— Section  near  Charleston,  W.  Va. 


As  may  be  seen  from  these  sections 
just  given,  many  of  the  beds  which  have 
received  distinct  names  are  not  persist- 
ent. They  occur  at  some  localities  but 
are  wanting  in  others,  and  hence  are  so 
variable  that  they  are  never  all  found  in 
one  section. 

We  shall  now  take  up  the  more  im- 
portant members  of  the  series  and  de- 
scribe them  in  more  detail  as  exhibited  at 
their  type  localities  and  elsewhere. 


86 


THE  NORTHERN  BITUMINOUS  COAL  FIELD. 


[BULL.  65. 


CHARACTERISTIC  HORIZONS. 


THE  PITTSBURGH  COAL  ORES. 


In  Fayette  County,  Pennsylvania,  a group  of  iron  ores  come  immedi- 
ately below  the  Pittsburgh  coal,  and  have  been  mined  for  the  manufac- 
ture of  iron  for  nearly  75  years.  They  have  been  very  carefully  studied 
by  Stevenson,  who  describes  them  in  his  report  (KK)  of  the  Pennsylva- 
nia Geological  Survey.  He  gives  the  following  as  the  general  section 
of  the  ores : 


Pittsburgh  coal 

Clay 

Blue  Lump  ore 

Clay ... 

Condemned  flag  ore 

Clay 

Big  Bottom  ore 

Clay 

Red  flag  ore 

Clay 

Yellow  flag  ore 


2 to  8 feet. 

1 to  0 foot. 

4 inches  to  1 foot  6 inches. 

1 to  0 foot. 

. 4 inches  to  2 feet  6 inches. 
...1  foot  to  1 foot  8 inches. 

10  inches  to  5 feet. 

2 inches  to  6 feet. 

1 to  3 feet. 

4 inches. 


This  succession  does  not,  of  course,  represent  the  structure  of  the  ore 
layers  at  all  localities,  as  the  thickness  and  quality  are  constantly  vary- 
ing. 

The  “ Blue  Lump  ” and  the  “ Big  Bottom  ” beds  are  of  the  most  im- 
portance, and  it  is  from  the  former  one  especially  that  Mr.  F.  H.  Oli- 
phant  manufactured  iron  so  long  and  successfully  at  Fairchance. 
These  ores  are  confined  principally  to  the  Blairsville  basin,  in  Fayette 
County,  though  they  extend  into  the  edge  of  Monongalia  County  to  the 
south,  and  have  been  recognized  on  the  edge  of  Greene  County  to  the 
west. 

When  these  ores  are  not  present  their  places  are  often  occupied  by 
ferruginous  limestones  or  shales,  though  occasionally  a sandstone 
stratum  comes  in  close  under  the  coal  and  cuts  out  everything  else. 
This  interval,  immediately  below  the  Pittsburgh,  for  30  to  40  feet  is 
more  variable  than  any  other  portion  of  the  Barrens,  and  hence  it  is 
useless  to  attempt  to  classify  its  rocks. 


THE  LITTLE  PITTSBURGH  COAL. 

At  a varying  interval  of  25  to  60  feet  from  the  top  of  the  Barrens 
there  often  occurs  a thin  and  usually  impure  coal  bed,  which  has  been 
termed  the  Little  Pittsburgh  coal,  from  the  fact  that  it  is  so  close  to 
the  great  bed  above.  The  thickness  selc.om  exceeds  two  feet,  and  it  is 
often  only  half  that.  The  best  development  of  this  coal  which  the 
writer  has  ever  seen  occurs  in  Fairfax  Knob,  Tucker  County,  West  : 
Virginia,  at  the  locality  of  Section  45,  where  the  bed  is  nearly  4 feet 
thick  and  is  locally  known  as  the  “ coking  vein,”  from  the  fact  that  it 
has  the  typical  structure  of  a good  coking  coal. 

• 

M 


WHITE.] 


THE  BARREN  MEASURES. 


87 


Occasionally  there  appear  to  be  two  of  these  beds,  one  at  20  to  30 
feet  below  the  Pittsburgh  and  the  other  at  50  to  75  feet  below,  but 
they  may  probably  both  be  splits  from  the  same  bed. 

The  Little  Pittsburgh  coal  is  quite  persistent  at  the  northern  end  of 
the  Appalachian  coal  basin,  but  it  disappears  south  westward  across 
West  Virginia  and  is  seldom  seen  beyond  Harrison  County.  It  also 
fades  away  southward  in  Ohio,  since  it  does  not  appear  in  any  of  the 
Ohio  sections,  unless  it  should  be  the  “ Jeffers”  coal  of  Prof.  Andrews, 
in  Gallia  County.  That,  however,  may  possibly  represent  the  Pitts- 
burgh bed.  In  the  vicinity  of  Wellersburg,  Somerset  County,  Penn- 
sylvania, there  appear  to  be  two  of  these  Little  Pittsburgh  beds,  and 
the  upper  contains  3 to  4 feet  of  good  coal,  while  the  lower  is  only  18 
inches  thick. 

THE  PITTSBURGH  LIMESTONES. 

There  are  very  frequently  two  limestones  in  the  shale  interval  of  50 
to  75  feet  below  the  Pittsburgh  coal,  one  of  which  comes  above. the 
Little  Pittsburgh  coal  and  the  other  a few  feet  below.  They  are  both 
known  under  the  general  name  of  Pittsburgh  limestone ; but  it  would 
be  better  to  call  the  first  one  Upper  Pittsburgh  and  the  other  one 
Lower  Pittsburgh.  The  first  is  seldom  more  than  3 to  5 feet  thick,  but 
the  latter  is  occasionally  much  thicker,  as  it  is  the  more  persistent  of 
the  two,  being  purer  and  frequently  quarried  and  burned  into  lime  for 
agricultural  and  other  purposes. 

THE  CONNELLSVILLE  SANDSTONE. 

At  a short  interval  under  the  Lower  Pittsburgh  limestone  there  is 
often  found  a massive  sandstone  which  is  frequently  conglomeritic. 
This  rock  rises  from  the  bed  of  the  Youghiogheny  River  at  Counells- 
ville,  and  was  named  from  that  locality  by  Dr.  Stevenson.  Being  one 
of  the  cliff  rocks  in  the  Barren  Measures,  it  has  played  an  important 
part  in  shaping  their  topography.  It  is  especially  hard  and  massive 
in  the  Cumberland  or  Georges  Creek  basin,  and  the  rounded  hills 
which  hold  the  “Big”  (Pittsburgh)  “vein”  rest  on  a platform  of  this 
rock,  which,  owing  to  its  erosion-resisting  power,  makes  a bold  terrace 
far  uj)  the  mountain  sides  after  all  the  soft  beds  above  have  disappeared. 
It  is  this  great  bed  of  pebbly  sandstone  that  caps  the  summits  in  the 
center  of  the  trough  south  from  Elk  Garden,  after  the  Pittsburgh  coal 
has  disappeared,  forming  almost  level  plateaus  over  thousands  of  acres 
where  the  great  Pittsburgh  bed  is  missed  by  an  interval  of  only  50  to 
60  feet. 

The  same  pebbly  sandstone  marks  the  summits  of  the  hills  at  Beling- 
ton,  Barbour  County,  West  Virginia,  and  forms  huge  cliffs  at  many 
points  along  the  Monongahela  River  between  Fairmont  and  Morgan- 
town. 

At  Connellsville  the  top  of  this  stratum  lies  about  60  feet  under  the 
Pittsburgh  coal ; but  this  interval  is  sometimes  as  small  as  40  feet,  and 


88 


THE  NORTHERN  BITUMINOUS  COAL  FIELD. 


[mull.  65. 


again  increases  to  80  or  90.  When  not  pebbly  it  frequently  furnishes 
excellent  building  stone.  The  thickness  varies  from  25  to  50  feet,  but 
it  is  often  absent  as  a massive  rock,  and  then  its  place  is  filled  with 
sandy  shales  or  flaggy  sandstone. 

THE  LITTLE  CLARKSBURG  COAL. 

By  this  name  has  been  designated  a bed  of  slaty  coal  which  occa- 
sionally makes  its  appearance  close  under  the  Connellsville  sandstone, 
and  100  to  125  feet  below  the  Pittsburgh  coal. 

At  Clarksburg,  West  Virginia,  the  coal  in  question  crops  out  along 
the  bed  of  Elk  Creek  for  a considerable  distance,  and  is  1J  to  2 feet 
thick,  but  poor  and  slaty.  It  is  called  Little  Clarksburg  to  distinguish 
it  from  the  Pittsburgh  coal,  which  is  extensively  mined  in  the  vicinity 
of  that  town,  and  is  locally  known  as  the  Clarksburg  bed. 

Very  frequently  this  coal  is  represented  by  a bed  of  black  slate, 
which  is  filled  with  fish  remains,  teeth,  scales,  etc.  The  deposit  in 
question  is  rarely  more  than  1J  to  2 feet  thick,  and  is  often  absent 
altogether,  so  that  it  is  of  very  little  economic  importance,  though  in 
the  Wellersburg  region  of  Somerset  County,  Pennsylvania,  it  attains 
a thickness  of  nearly  6 feet,  and  contains  some  good  coal,  being  known 
as  the  “G-foot”  bed. 

THE  CLARKSBURG  LIMESTONE. 

Directly  under  the  last  described  coal  there  often  occurs  a limestone 
which  is  finely  exposed  in  the  vicinity  of  Clarksburg,  along  the  bed  of 
Elk  and  the  West  Fork  Biver.  The  upper  portion  is  there  rather 
slaty,  and  filled  with  fossil  ostracoids  and  fish  remains.  The  next  layers 
under  this  are  very  compact,  and  come  out  in  peculiar  rhomboidal 
blocks.  This  entire  limestone  series  is  20  to  30  feet  thick,  and  some  of 
the  layers  are  quite  ferruginous,  so  much  so  that  they  were  mined  for 
ore  many  years  ago  at  an  old  charcoal  furnace  on  Elk.  Some  iron  ore 
was  also  obtained  near  Clarksburg  from  the  roof  shales  just  above  the 
Little  Clarksburg  coal,  and  used  in  this  furnace.  The  Clarksburg 
limestone  is  rather  widely  distributed  in  Pennsylvania  and  northern 
West  Virginia,  and  is  frequently  mined,  since  many  of  its  layers  fur- 
nish good  lime  for  fertilizing  and  building  purposes. 

THE  MORGANTOWN  SANDSTONE. 

At  25  to  40  feet  under  the  Clarksburg  limestone,  and  separated  from 
it  by  soft  shales,  we  find  one  of  the  great  sandstone  horizons  of  the 
Barren  Measures.  This  rock  was  named  by  Dr.  Stevenson  from  its 
fine  exposure  at  Morgantown,  West  Virginia,  where  it  has  been  exten- 
sively quarried  and  used  in  building  the  State  University  and  other 
structures.  At  this  typical  locality  the  top  of  the  stratum  lies  about 
200  feet  below  the  Pittsburgh  coal,  and  the  thickness  of  the  sandstone 
is  25  feet.  It  is  of  a yellowish  gray  cast,  of  medium  grain  and  hard- 
ness, and  splits  readily  into  blocks  of  any  desirable  size.  Scattered 


WHITE.] 


THE  BARREN  MEASURES. 


89 


through  the  rock  are  stains  of  peroxide  of  iron  and  also  a considerable 
quantity  of  feldspar  graius,  which  are  generally  decomposed,  thus 
giving  the  surface  of  the  stone  a mealy  look.  In  some  of’ the  crevices 
and  cavities  of  the  sandstone  pure  kaolin  has  accumulated  from  this 
source.  The  base  of  the  sandstone  is  often  conglomeritic  and  some- 
times brecciated. 

This  is  a quarry  sandstone  nearly  everywhere  that  its  outcrop  ex- 
tends. All  along  the  Monongahela  River  it  has  been  quarried  and 
used  in  building  the  locks  of  the  Slack  Water  Company.  The  stone 
dam,  No.  9,  was  built  of  rock  from  this  stratum.  It  is  one  of  the  most 
persistent  members  of  the  Barren  Measures,  and  often  makes  high 
cliffs.  It  caps  the  hills  in  the  vicinity  of  Grafton,  West  Virginia, 
where  it  is  also  quarried,  and  it  makes  a line  of  conspicuous  bluffs  from 
there  to  beyond  Newburg,  along  Three  Fork,  and  far  up  into  Barbour 
County  along  the  Valley  River.  Along  the  North  Potomac  River,  in 
Mineral,  Grant,  and  Garrett  Counties,  the  same  rock  is  found,  and  on 
the  Great  Kanawha,  Guyandotte,  Big  Sandy,  Big  and  Little  Muskin- 
gum, and  other  tributaries  of  the  Ohio,  this  bed  is  generally  conspicu- 
ous. At  Huntington,  West  Virginia,  on  the  banks  of  the  Ohio,  it  is  50 
to  60  feet  thick,  while  on  Crooked  Run,  Monongalia  County,  near  the 
Pennsylvania  line,  the  stratum  is  100  feet  thick.  It  is  the  first  oil  rock 
on  Dunkard  Creek,  and  some  of  the  wells  produced  largely  from  it.  In 
the  deep  borings  of  Washington  County,  Pennsylvania,  where  it  under- 
lies the  surface  500  to  1,000  feet,  this  stratum  is  35  to  50  feet  thick,  and 
generally  contains  salt  water. 

THE  ELK  LICK  COAL. 

Immediately  under  the  Morgantown  sandstone,  or  separated  from  it 
by  only  a few  feet  of  shale,  there  comes  a coal  of  very  wide  distribution 
which  occasionally  attains  workable  dimensions. 

This  name  was  given  the  coal  in  question  by  the  First  Geological  Sur- 
vey of  Pennsylvania,  but  the  place  of  the  bed  in  the  series  remained 
uncertain  till  Messrs.  Platt,  of  the  Second  Survey,  recently  deter- 
mined the  matter  finally  by  identifying  the  massive  sandstone  above  it 
at  the  typical  locality  as  the  Morgantown. 

This  coal  attains  a thickness  of  4 feet  in  Somerset  County,  Penn- 
sylvania, and  has  there  been  mined  to  a considerable  extent  for  local 
use. 

In  Westmoreland,  Fayette,  and  Alleghany  it  seldom  exceeds  2 feet, 
and  is  generally  less,  but  quite  persistent. 

In  Preston  County,  West  Virginia,  north  from  Cheat  River,  this  bed 
has  been  mined  to  a considerable  extent  and  is  known  as  the  u top 
vein.”  In  the  summits  near  Bruceton  it  is  4 feet  thick  and  a rather 
good  coal. 

At  Morgantown  it  is  nearly  4 feet  thick,  but  rather  poor  and  slaty. 

South  from  Monongalia  County,  it  is  occasionally  seen,  but  is  not  so 


90 


THE  NORTHERN  BITUMINOUS  COAL  FIELD. 


[bull.  65. 


thick  as  at  the  northern  end  of  the  field.  At  Glenville,  Gilmer  County, 
it  is  in  the  bed  of  the  Little  Kanawha  Biver,  and  18  to  20  inches  thick. 

The  same  coal  is  also  recognizable  on  the  Big  Kanawha,  but  is  there 
quite  thin.  In  the  section  (48)  at  Huntington,  West  Virginia,  Mr. 
Selby  finds  this  coal  2 feet  thick  but  very  slaty. 

It  is  not  often  reported  by  the  Ohio  geologists,  and  hence  may  fre- 
quently be  absent  from  the  measures  in  that  State. 

THE  ELK  LICK  LIMESTONE. 

In  sections  37  and  43,  a limestone  is  seen  at  a short  interval  below 
the  Elk  Lick  coal,  and  from  its  occurrence  at  this  hori  zon  in  Somerset 
County,  Pennsylvania,  it  has  been  termed  the  Elk  Lick  limestone  by 
Mr.  Franklin  Platt,  of  the  Second  Geological  Survey,  Pennsylvania. 
The  stratum  in  question  occurs  at  200  to  240  feet  under  the  Pittsburgh 
coal,  and  is  not  always  present. 

As  exhibited  in  Somerset  County,  Pennsylvania,  this  limestone  is  of 
a light  gray  color,  and  often  tinged  with  buff,  the  same  being  true  of  it 
in  Monongalia.  Platt  reports  it  as  12  feet  thick  in  Somerset,  but  in 
Monongalia  it  is  only  about  half  that,  and  is  not  persistent. 

THE  CRINOIDAL  LIMESTONE  (GREEN  FOSSILIFEROUS  LIMESTONE,  AMES  LIMESTONE). 

The  next  step  downward  in  the  rocks  takes  us  to  a very  important 
horizon  and  one  which  marks  a change  from  fresh  or  brackish  water 
deposits  to  marine  conditions,  for  here  we  get  abundant  marine  fossils 
for  the  first  time  in  descending  the  column  of  rocks. 

The  bed  in  which  these  fossils  occur  has  received  several  names. 
The  geologists  of  the  First  Geological  Survey  of  Pennsylvania  called 
it  the  Green  Fossiliferous  limestone,  the  Ohio  Survey  has  termed  it  the 
Ames  limestone,  while  the  Second  Geological  Survey  of  Pennsylvania 
has  termed  it  the  Crinoidal  limestone.  This  latter  name  is  so  well 
known  now  in  geological  literature  that  it  is  probably  best  to  let  it  stand, 
though  as  a synonym  and  geographical  designation  the  Ames  lime- 
stone may  be  retained. 

The  character  of  this  stratum  and  its  fossils  have  been  admirably 
worked  out  by  Stevenson,  who  first  showed  its  importance  as  a strati- 
graphical  horizon.  It  comes  almost  exactly  midway  in  the  Barren 
series,  and  hence  it  is  a constant  datum  from  which  the  geologist  can 
measure  either  upward  or  downward  to  identify  the  rocks. 

When  once  thoroughly  known  it  can  not  be  confused  with  any  other 
rock  in  these  measures,  since  it  is  the  highest  bed  that  coutains  abun- 
dant Brachiopods  and  Lamellibranclis,  and  its  lithology  is  distinctly  dif- 
ferent from  anything  else.  Prof.  Stevenson  thus  aptly  describes  its 
general  features : “ Dark  bluish  or  greenish  gray,  tough,  and  breaks 
with  a granular  surface  much  resembling  that  of  a coarse  sandstone. 
* * *.  In  all  cases  it  is  fossiliferous  and  contains  immense  numbers 

of  crinoidal  stems  and  spines  or  plates.” 


WHITE.) 


THE  BxlRREN  MEASURES. 


91 


Its  common  fossils  are:  Productus  Nebrascensis , P.  Prattenianus , P. 
longispinus , P.  semi-reticulatus , Hemipronites  crassns,  Spirifera  earner  ata, 
S.  piano  eonvexa,  Athyris  subtilita , Lophophyllum  proliferum , Zeacrinus 
mucrospinus , together  with  the  undetermined  plates  and  stems  of  cri- 
noids. 

Throughout  Pennsylvania  this  stratum  comes  about  275  to  300  feet 
below  the  Pittsburgh  coal,  and  the  same  distance  above  the  Upper 
Preeport,  though  occasionally  this  last  interval  is  increased  to  350  feet. 
The  rock  is  rarely  more  than  2 feet  thick,  and  often  not  so  much,  but  is 
wonderfully  persistent.  Even  when  not  present  as  limestone  its  hori- 
zon is  almost  invariably  made  known  by  the  fossiliferous  shales  which 
accompany  the  bed. 

Through  Ohio  thjs  rock  is  almost  continuously  present  from  the  point 
where  it  enters  the  State  near  Steubenville  clear  around  to  where  it 
leaves  it  at  the  Kentucky  line  near  Catlettsburg. 

Opposite  Steubenville  the  bed  is  8 to.10  feet  thick,  but  this  is  unusual, 
since  it  is  only  1 to  3 feet  at  most  points  in  Ohio. 

The  interval  between  this  rock  and  the  Pittsburgh  coal  decreases 
westward  to  200  feet  on  the  Ohio  River  at  Wellsburg,  and  farther  west 
in  Ohio  the  interval  still  further  declines  to  140  feet,  but  where  it  leaves 
the  State  at  the  southwest  it  increases  again  and  gets  to  be  300  feet 
opposite  Huntington,  West  Virginia. 

Through  this  latter  State  the  limestone  holds  its  place  very  regularly 
in  the  series  from  the  Pennsylvania  line  southward  into  Harrison  and 
Lewis  Counties,  and  it  is  also  present  on  the  Volcano  uplift  at  Burn- 
ing Springs  and  other  points,  still  holding  its  characteristic  fossils.  It 
disappears,  however,  in  passing  from  this  Little  Kanawha  region  south- 
ward to  the  Big  Kanawha,  for  when  we  come  to  this  latter  stream  the 
fossiliferous  limestone  is  gone,  and  its  horizon  replaced  near  Charles- 
ton by  a thin,  impure  limestone  which  holds  only  minute  fresh  water 
forms.  It  is  highly  probable,  however,  that  the  crinoidal  bed  comes  in 
again  a few  miles  north  from  Charleston,  since  on  the  Big  Sandy  it  was 
followed  20  to  25  miles  above  the  mouth  of  that  stream,  and  there  it 
still  retains  its  crinoidal  phase,  though  getting  very  impure  where  last 
seen  in  that  valley. 

THE  CRINOIDAL  COAL. 

Immediately  under  the  last  described  limestone  we  very  often  find  a 
thin  coal  bed,  which  seldom  exceeds  18  inches  in  thickness,  and  hence 
is  of  very  little  economic  importance.  In  Somerset  County,  Pennsylva- 
nia, Mr.  Franklin  Platt  identified  with  this  coal  No.  8 of  the  Berlin  (37) 
section,  a very  impure,  slaty  bed,  occurring  in  several  layers  in  the  vi- 
cinity of  Berlin,  where  it  is  altogether  7 feet  thick,  and  locally  known 
as  the  Platt  coal.  If  this  identification  be  correct,  this  is  the  greatest 
development  the  coal  ever  attains. 

There  is  only  one  other  locality  besides  the  Berlin  region  where 
this  coal  has  been  mined  to  any  considerable  extent,  and  that  is  at 


92 


THE  NORTHERN  BITUMINOUS  COAL  FIELD. 


[BULL.  65. 


Burning  Springs,  Wirt  County,  West  Virginia.  Here  it  was  mined 
aud  used  for  fuel  iu  drilling  the  numerous  oil  wells  once  put  down  there, 
and  it  is  still  taken  out  on  a small  scale  for  domestic  purposes,  though 
only  20  inches  thick.  Some  very  finely  preserved  fossil  Brachiopods 
and  Lamellibrauchs  have  been  obtained  from  the  roof  shales  of  the 
coal  at  Burning  Springs,  since  it  there  comes  only  2 to  5 feet  below  the 
Crinoidal  liihestone. 

The  u Weller”  coal,  near  Wellersburg,  Pennsylvania,  is  probably 
identical  with  this  bed. 

RED  SHALE  BEDS. 

Throughout  most  of  the  Pennsylvania  and  West  Virginia  region,  the 
Crinoidal  limestone  is  underlaid  by  very  soft,  red,  and  variegated  shales, 
and  marly  clays.  They  make  a broad  red  band  in  the  soil  wherever 
they  extend,  and  are  a great  nuisance  along  roads  and  railroads,  since 
when  wet  they  decompose  into  a greasy  mud,  which  produces  many 
landslides  and  slips. 

It  is  this  stratum  which  causes  so  much  trouble  to  the  oil  and  gas 
drillers  of  southwestern  Pennsylvania  aud  the  adjoining  regions  of 
West  Virginia,  since  it  is  so  easily  reduced  to  mud,  which  runs  into  the 
hole  and  fills  it  up,  so  that  casing  must  be  put  through  the  stratum  as 
soon  as  the  drill  has  penetrated  it.  From  this  tendency  to  slide  out 
into  the  drill  hole,  it  is  termed  by  the  oil  drillers  the  u caving”  rock. 

Over  a large  portion  of  Ohio  and  in  many  regions  of  West  Virginia 
a hard,  bluish  gray  limestone,  not  at  all  or  but  sparingly  fossiliferous, 
occurs  near  the  center  of  this  shale  interval.  The  bed  is  3 to  10  feet 
thick,  and  in  Ohio  is  generally  called  the  Ewing  limestone.  It  is  shown 
in  the  West  Virginia  sections  at  Burning  Springs  (47)  and  at  Hunting- 
ton  (48),  and  it  is  recognizable  at  many  other  points  in  the  State. 

The  rest  of  the  Barren  Measures  from  this  red  shale  down  to  the  Ma- 
honing sandstone  is  extremely  variable.  ’Sometimes  it  is  nearly  all 
shales,  much  of  which  is  red,  and  u caves  ” in  drilling  through  it,  just 
like  that  under  the  Crinoidal  limestone,  and  again  as  in  the  Berlin  sec- 
tion (37)  it  contains  3 or  4 coal  beds,  and  as  many  limestones.  Some  of 
these,  however,  are  rather  persistent  and  will  be  referred  to  in  detail. 

THE  BAKERSTOWN  COAL. 

At  some  localities  in  western  Pennsylvania  a bed  of  coal  is  found  75 
to  90  feet  uuder  the  Crinoidal  limestone.  This  bed  is  mined  in  the  vi- 
cinity of  Bakerstown,  Alleghany  County,  and  it  has  been  designated 
from  that  village.  As  there  exhibited,  it  is  not  quite  3 feet  thick  and 
rather  slaty.  In  the  Berlin  region  a coal  called  the  Price  bed  seems  to 
come  at  this  horizon.  It  is  about  4 feet  thick  and  furnishes  some  val- 
uable fuel  in  Somerset  County. 

Iu  Section  37  will  be  found  some  thin  coal  beds  under  the  Price  coal, 
which  are  rarely  represented  in  any  other  section  of  the  Barrens. 


WHITE.] 


THE  BARREN  MEASURES. 


93 


Among  these  are  the  Coleman,  Philson,  and  the  one  a few  feet  under 
the  Price  bed;  but  they  are  all  local,  though  occasionally  we  find  traces 
of  some  of  them  in  other  regions  than  Somerset  County.  This  whole 
interval  for  100  feet  below  the  Crinoidal  limestone  is  so  extremely  vari- 
able that  the  classification  for  one  region  is  of  very  little  use  in  another. 
An  instance  of  this  is  seen  at  Saltsburg,  Pennsylvania,  where  a great 
sandstone  100  feet  thick  comes  into  the  series  a few  feet  under  the 
Crinoidal  limestone  horizon.  This  was  termed  the  Saltsburg  sandstone 
by  Stevenson,  but  it  is  hardly  persistent  enough  to  classify  as  a regu- 
lar member  of  the  Barrens.  In  the  Charleston,  West  Virginia,  region 
a massive  pebbly  sandstone  occurs  not  far  from  the  horizon  of  the 
Saltsburg  rock,  and  the  one  which  caps  the  hills  at  the  mouth  of  the 
Big  Sandy  River  may  be  identical  with  the  same  bed. 

THE  CAMBRIDGE  LIMESTONES. 

At  many  localities  in  Ohio  two  dark  fossiliferous  limestones  occur 
only  20  to  30  feet  apart,  and  Prof.  Orton,  director  of  the  Ohio  Geologi- 
cal Survey,  has  named  them  respectively  the  Upper  and  Lower  Cam- 
bridge limestones.  In  Ohio  these  beds  generally  occur  from  90  to  130 
feet  under  the  Crinoidal  limestone  and  are  always  very  fossiliferous. 

In  many  regions  of  Pennsylvania  two  dark  fossiliferous  limestones 
occur,  which  correspond  to  the  two  in  Ohio,  only  there  they  are  60  to 
70  feet  apart,  and  the  upper  one  90  to  120  feet  under  the  crinoidal  bed, 
while  the  lower  one  is  150  to  190  feet  below  the  same  horizon.  1 have 
identified  the  two  in  Pennsylvania  with  the  two  in  Ohio,  and  have  also 
adopted  the  Ohio  names,  since  the  Pennsylvania  beds  are  known  under 
several  names  in  different  parts  of  the  field,  while  the  Ohio  names  are 
now  well  established.  The  upper  one  is  the  lighter  colored  of  the  two, 
and  while  generally  fossiliferous,  the  fossils  are  not  so  abundant  as  in 
the  lower  limestone.  This  upper  one  was  termed  the  Pine  Creek  lime- 
stone in  my  Report  Q of  the  Pennsylvania  Survey,  while  in  Somerset 
County  it  seems  to  be  identical  with  the  Coleman  limestone  of  Platt. 

At  Morgantown,  West  Virginia  (Section  42),  this  bed  is  dark,  quite 
fossiliferous,  and  lies  85£  feet  below  the  Crinoidal  limestone. 

The  term  Black  Fossiliferous  limestone  of  the  First  Pennsylvania 
Geological  Survey  Reports  was  probably  applied  quite  as  often  to  this 
upper  rock  as  to  the  lower  one,  since  at  times  they  very  closely  re- 
semble each  other,  and  contain  practically  the  same  fossils. 

The  interval  separating  the  two  limestones  is  generally  shale  in  Ohio, 
but  in  Pennsylvania  it  is  sometimes  a massive  sandstone,  and  60  to  90 
feet  thick. 

The  Lower  Cambridge  limestone  is  identical  with  the  one  termed 
Brush  Creek  limestone  by  the  writer  in  Report 'Q,  Second  Geological 
Survey  of  Pennsylvania,  but  the  geological  horizon  of  that  limestone 
was  there  placed  lower  than  it  should  have  been  by  50  to  60  feet,  since 
it  was  considered  to  belong  between  the  two  members  of  the  Mahoning 


94 


THE  NORTHERN  BITUMINOUS  COAL  FIELD. 


[BULL.  65. 


sandstone,  instead  of  above  both  members,  and  hence  the  term  Brush 
Greek  limestone  should  be  dropped  from  the  nomenclature,  and  Lower 
Cambridge  substituted.  This  lower  limestone  is  very  fossil iferous, 
often  being  a mere  mass  of  Brachiopods  and  Lamellibranchs,  of  which 
the  most  common  are  Chonetes  mesoloba , Athyris  subtilita , Pruductus 
Nebracensis  and  a large  Solenomya,  together  with  Nautiliis  occidentalis 
and  Orthoceras  cribrosum. 

This  bed  seems  to  be  quite  as  persistent  in  Ohio  as  the  Crinoidal 
limestone,  since  it  is  present  in  almost  every  section  at  the  proper 
horizon,  from  Steubenville  clear  around  to  fronton,  near  which  latter 
poiut  it  is  only  75  feet  above  the  base  of  the  Barrens. 

In  the  hills  at  Catlettsburg,  Kentucky,  a dark  fossiliferous  limestone 
occurs  at  160  feet  above  the  Upper  Freeport  coal,  but  this  is  probably 
the  Upper  Cambridge,  and  the  same  limestone  occurs  in  the  summits 
of  the  hills  opposite  Louisa,  Kentucky,  at  200  feet  above  the  Upper 
Freeport  bed.  It  is  barely  possible,  however,  that  this  may  be  the 
Lower  Cambridge  limestone,  since  the  Barrens  thicken  very  rapidly 
southward  from  their  northwestern  outcrop.  In  the  Berlin  section, 
(37),  the  Lower  Cambridge  limstone  appears  to  be  represented  by  the 
Philson  limestone  of  Platt.  The  “ calcareo- siliceous  rock”  of  Hildreth, 
in  Ohio,  appears  to  represent  the  same  bed. 

THE  MASONTOWN  COAL. 

At  an  interval  of  5 to  20  feet  below  the  Lower  Cambridge  lime- 
stone there  occurs  a coal  bed  which  has  quite  a wide  distribution.  It 
attains  its  best  development  in  the  region  of  Masontown,  Preston 
County,  West  Virginia,  and  it  has  been  designated  from  that  village. 
It  is  there,  and  at  many  other  points  in  the  Preston  basin,  mined  for 
domestic  purposes,  being  known  as  the  u 4-foot”  bed,  and  is  a dry, 
open-burning  coal,  highly  prized  for  domestic  fuel.  It  is  everywhere 
preferred  to  the  Upper  Freeport,  which  is  accessible  in  the  same 
region. 

This  appears  to  be  the  same  bed  which  the  writer  described  in  Re- 
port Q,  Second  Geological  Survey  of  Pennsylvania,  under  the  n^ine  of 
Brush  Creek  coal,  since  a diamond  drill  hole  has  recently  shown  that 
the  Brush  Creek  bed  lies  135  feet  above  the  Upper  Freeport  coal  instead 
of  75,  as  formerly  supposed,  and  hence  it  is  deemed  best  to  drop  the 
name  Brush  Creek  altogether  for  both  the  coal  and  the  limestone. 
This  Masontown  coal  is  generally  the  first  one  above  the  top  of  the 
Mahoning  sandstone,  and  the  interval  separating  it  from  the  latter  varies 
from  5 to  50  feet.  Very  frequently  the  coal  is  only  one-half  to  1 foot 
thick,  and  sometimes  it  is  represented  only  by  black  slate. 

Near  Gallitzin,  Pennsylvania,  it  is  seen  in  a cut  on  the  old  Por- 
tage Railroad,  where  it  is  only  one-half  foot  thick,  but  it  is  overlaid  by 
3 to  4 feet  of  black  slate.  The  coal  is  here  140  feet  above  the  Upper 


WIUTK.J 


THE  BARREN  MEASURES. 


95 


Freeport  coal  as  measured  in  the  McCoy  shaft,  which  starts  at  the  horn 
zon  of  the  Masontown  bed. 

This  coal  is  reported  as  present  at  many  localities  in  Ohio,  though 
there  it  seldom  exceeds  2 feet  in  thickness.  It  is  probably  this  bed 
which  has  been  opened  near  the  summit  of  the  hill  opposite  Louisa, 
Kentucky,  where  it  is  2 feet  thiek  and  rather  slaty. 

In  the  Beliugton  basin,  Barbour  County,  West  Virginia,  this  coal 
attains  a fine  development  and  is  often  4 to  5 feet  thick  with  6 inches 
of  bony  coal  near  the  center. 

THE  IRONDALE  LIMESTONE  AND  ORE. 

Directly  under  the  Masontown  coal  there  is  occasionally  found  a bed 
of  huffish  gray  limestone,  which  at  Irondale,  Preston  County,  West 
Virginia,  and  adjoining  regions,  is  accompanied  by  a bed  of  iron  ore 
immediately  under  the  limestone. 

When  the  ore  is  present,  however,  the  coal  above  is  generally  absent, 
as  is  the  case  at  Irondale  and  Gladeville,  Preston  County,  where  the  ore 
has  been  used  to  a considerable  extent.  It  varies  in  thickness  frotn  1 
to  2 feet,  and  is  rather  siliceous,  there  being  only  about  38  per  cent  of 
metallic  iron  in  the  ore.  It  comes  155  feet  above  the  Upper  Freeport 
coal,  and  hence  its  horizon  is  assigned  to  that  of  the  Masontown  coal, 
since  the  interval  agrees,  and  then  a similar  limestone  3 feet  thick  is 
seen  under  the  coal  at  Albright  and  other  localities  in  Preston  County. 

THE  MAHONING  SANDSTONE. 

This  is  the  lowest  sandstone  deposit  of  the  Barren  Measures,  and  al- 
though at  times  consisting  of  one  solid  rock,  yet  it  is  generally  complex. 
The  usual  rule  is  for  the  mass  to  divide  into  two  sandstones,  an  Upper 
and  Lower  Mahoning,  each  40  to  50  feet  thick,  with  a shale  interval 
between  containing  a coal  bed  and  limestone  or  iron  ore,  but  sometimes 
when  the  group  reaches  a great  development,  as  on  the  Big  Kanawha 
(Section  49),  it  contains  three  coal  beds,  and  as  many  sandstone  divi- 
sions. This  is  exceptional,  however,  the  normal  structure  having  only 
two  sandstones  with  one  included  coal,  the  whole  series  being  100  to 
150  feet  thick. 

The  wild  scenery  and  poor  soil  of  the  lower  portion  of  the  Barrens 
are  largely  due  to  these  sandstones.  Being  frequently  quite  hard  and 
even  pebbly,  they  cap  the  hills  long  after  all  the  other  members  of  the 
Barrens  above  have  disappeared,  and  they  have  thus  protected  the 
underlying  Lower  Coal  Measures  over  wide  areas  where  the  latter 
would  otherwise  have  been  carried  away  by  erosion. 

In  Wyoming  County,  West  Virginia,  they  cap  the  summits  of  Guy- 
ahdotte  Mountain  at  an  elevation  of  3,000  feet  above  the  sea.  Much  of 
the  Lower  ( oal  Measures  between  that  mountain  and  the  Great  Ka- 
nawha River  would  have  been  swept  away  but  for  this  massive  coping. 

It  is  the  same  friendly  cover  that  has  preserved  large  areas  of  the 


96 


THE  NORTHERN  BITUMINOUS  COAL  FIELD. 


[BULL  65. 


Coal  Measures  on  the  summits  of  the  Alleghany  Mountains,  and  in  iso- 
lated basins  like  Broad  Top.  The  great  tunnels  on  the  Pennsylvania 
and  Baltimore  and  Ohio  Railroads,  Gallitzin  and  Kingwood  respect- 
ively, pass  under  domes  of  this  sandstone  group.  Some  portious  of 
this  sandstone  nearly  always  furnish  good  building  rock,  the  Govern- 
ment locks  on  the  Great  Kanawha  being  constructed  of  it.  The  same 
stone  is  also  largely  quariied  along  the  Ohio  River  hills  in  Beaver 
County,  Pennsylvania. 

The  Upper  Mahoning  is  generally  more  massive  than  the  Lower  one, 
and  is  the  conglomeritic  member,  since  it  is  often  a mere  mass  of  quartz 
pebbles,  having  once  been  quarried  for  mill  stones  on  Cheat  River  near 
Morgantown.  In  the  Great  Kanawha  region  this  rock  is  extremely 
hard  and  siliceous,  and  at  many  points  a mere  bed  of  pebbles,  some  of 
which  are  as  large  as  an  egg. 

THE  MAHONING  COAL. 

This  is  the  coal  bed  which  is  so  often  bound  up  between  the  two 
great  divisions  of  the  Mahoning  sandstone.  It  was  formerly  called 
the  Brush  Creek  by  the  writer,  but  as  the  place  of  that  coal  was  mis- 
understood, it  is  thought  best,  as  already  stated,  to  drop  the  name  en- 
tirely, and  replace  it  with  the  name  Mahoning,  since  it  comes  in  the 
middle  of  the  Mahoning  sandstone.  It  is  possible  that  the  Gallitzin 
coal  of  Platt  in  Cambria  and  Blair  Counties  may  belong  at  this  horizon, 
but  owing  to  the  uncertainty  connected  therewith  it  has  been  deemed 
best  not  to  adopt  that  name. 

This  is  a very  widely  distributed  coal  bed,  and  frequently  attains 
commercial  importance.  It  is  the  coal  No.  7 of  the  eastern  Ohio  series, 
where  it  is  3 feet  thick  and  very  excellent  fuel.  It  is  mined  at  many 
localities  in  Ohio,  as  well  as  in  Pennsylvania. 

On  the  Great  Kanawha  River,  a few  miles  above  Charleston,  this  bed 
swells  out  to  a thickness  of  17  feet  in  the  vicinity  of  Coalburg ; but 
much  of  this  is  slate  and  bone,  there  being  only  5 to  6 feet  of  good  coal 
in  the  bed.  There  is  probably  a considerable  area  of  this  coal  of  mer- 
chantable thickness  in  the  region  southwest  from  the  Great  Kanawha, 
since  it  is  several  feet  thick  along  the  summits  of  ridges  in  the  Huff 
Creek  Mountains,  at  the  southern  line  of  Logan  County,  and  the  same 
bed  is  5 feet  thick  along  the  Tug  branch  of  Big  Saudy,  and  in  the 
Peach  Orchard  region  of  Kentucky,  where  it  occurs  235  feet  above  the 
Peach  Orchard  bed  (Winnifrede).  The  coal  is  quite  hard,  and  in  many 
places  a “ block”  coal  through  this  southwestern  region.  The  interval 
of  this  bed  above  the  base  of  the  Barren  Measures  varies  from  50  to 
175  feet,  this  latter  being  the  figure  at  Coalburg  and  Peach  Orchard. 

THE  MAHONING  LIMESTONE. 

Occasionally  a limestone  comes  into  the  series  immediately  under  the 
Mahoning  coal.  In  Beaver  County,  Pennsylvania,  it  is  often  5 to  8 feet 


WHITE.] 


THE  BARREN  MEASURES. 


97 


thick,  and  is  locally  termed  the  “ Summit”  limestone.  It  is  not  a per- 
sistent bed,  being  much  less  so  than  the  coal  of  the  same  name  above, 
and  when  present  it  is  often  impure  and  ferruginous.  In  fact  it  is  occa- 
sionally an  iron  ore,  the  Johnstown  ore  of  Pennsylvania  being  identical 
with  this  stratum. 

THE  UPPER  AND  MIDDLE  CANNELTON  COALS. 

Along  the  Great  Kanawha,  where  all  of  the  measures  have  thickened 
up  so  abnormally,  two  other  coal  beds  make  their  appearance  in  the 
Barren  series  below  the  Mahoning  coal,  and  they  have  been  termed  the 
Upper  and  Middle  Cannelton,  from  a locality  on  the  Kanawha  where 
both  .are  exposed.  The  former  has  there  been  mined  for  a long  time  in 
the  summit  of  the  hills,  where  it  furnishes  5 feet  of  excellent  “block” 
coal.  It  comes  90  feet  above  the  base  of  the  series,  but  the  interval 
constantly  decreases  northward,  and  at  Charleston  is  only  40  to  50 
feet.  As  this  interval  decreases  the  coal  becomes  inferior,  until  at 
Charleston  it  is  represented  by  some  coaly  streaks  only,  about  the  mid- 
dle of  the  Lower  Mahoning  sandstone. 

The  Middle  Cannelton  coal  never  attains  commercial  value,  and  is 
found  only  in  the  region  of  Cannelton  and  southward.  It  is  slaty, 
worthless,  never  more  than  3 feet  thick,  and  comes  20  to  25  feet  above 
the  base  of  the  Barrens. 

The  Lower  Mahoning  sandstone  is  generally  of  a bluish  gray  color, 
quite  homogeneous,  and  often  an  excellent  building  stone.  Though 
occasionally  containing  pebbles,  it  is  much  freer  from  them  than  the 
Upper  Mahoning.  The  thickness  varies  from  30  to  50  feet,  except  in 
the  Kanawha  region,  where  it  splits  up  into  two  or  three  divisions,  and 
is  more  than  100  feet  thick. 

The  shales  which  separate  the  Upper  and  Lower  Mahoning  sand- 
stones are  sometimes  red,  or  variegated,  as  in  the  Sewickley  section 
(34);  and,  occasionally,  as  in  the  vicinity  of  Tuunelton,  Preston  County, 
West  Virginia,  good  fire  clay  occurs  at  the  horizon  of  the  Mahoning 
limestone. 

Both  members  of  the  Mahoning  sandstone  are  occasionally  oil-pro- 
ducing, but  more  generally  the  upper  one,  this  being  the  main  oil  rock 
at  Bobtown,  on  Dunkard  Creek,  Greene  Couuty,  Pennsylvania,  and 
on  Whitely  Creek.  It  is  known  to  the  oil  producers  as  the  “Dunkard 
sand,”  and  it  is  also  oil-bearing  in  the  Macksburg  and  other  regions  of 
Ohio. 

The  shales  which  usually  intervene  between  the  base  of  the  Mahon- 
ing sandstone  and  the  Upper  Freeport  coal  often  contain  fossil  Brach- 
iopods  and  Lamellibrauchs,  as  well  as  the  common  coal  measure  plants. 
They  are  quite  variable  in  thickness,  the  Lower  Mahoning  sometimes 
cutting  out  the  shales  entirely  and  resting  on  the  Upper  Freeport  coal, 
while  again  the  shales  may  thicken  up  to  50  feet. 

Bull.  65 7 


98 


THE  NORTHERN  BITUMINOUS  COAL  FIELD. 


[BULL.  65. 


THE  KANAWHA  BLACK  FLINT. 

In  the  midst  of  the  shales  at  the  base  of  the  Barrens,  and  apparently 
at  the  horizon  which  usually  contains  the  marine  fossils,  there  occurs 
along  the  Great  Kanawha  River  a peculiar  deposit,  known  locally  as 
the  u Black  Flint.”  It  makes  its  appearance  in  the  section  first  at 
Charleston,  and  occurs  from  there  southward  along  the  river  until  the 
Barrens  disappear  from  the  summit  of  Gauley  Mountain,  50  miles  dis- 
tant. 

The  distribution  of  the  flint  appears  to  be  confined  to  a belt  along 
the  river  10  to  12  miles  wide,  since  at  5 to  0 miles  back  on  either  side  it 
generally  disappears  from  the  section,  so  as  to  be  no  longer  recogniza- 
ble. It  is  not  confined  to  the  Kanawha  region  however,  since  the 
deposit  is  visible  near  Clay  Court  House,  on  Elk  River,  and  near  the 
California  House,  on  the  crest  of  the  Burning  Springs  anticlinal,  where 
it  crosses  Hughes  River  at  the  corner  of  Wirt  and  Ritchie  Counties. 
The  rock  varies  from  5 to  15  feet  in  thickness,  and  is  usually  of  a dark 
or  bluish  black  color,  though  at  the  California  House  it  is  light  colored. 
Being  almost  indestructible  by  atmospheric  agencies,  it  has  played  a 
conspicuous  part  in  shaping  the  topography  in  the  Kanawha  region, 
since  it  protects  the  underlying  beds  from  erosion.  Through  the  agency 
of  heat  and  cold  it  finally  breaks  down  into  oblong  and  rudely  rectang- 
ular blocks  which  everywhere  line  the  beds  of  streams  and  cover  the 
surface  below  the  line  of  outcrop.  The  Indians  manufactured  arrow 
heads  and  other  implements  fr.)m  this  material,  so  that  pieces  of  it  have 
been  found  as  far  north  as  Pennsylvania.  It  is  evidently  a marine 
deposit,  since  it  is  distinctly  stratified,  and  specimens  of  Discina , Spi- 
rifera , and  Productus  are  common  in  the  less  siliceous  layers.  The  flint 
is  evidently  derived  from  the  skeletons  of  diatoms  aud  protozoa,  though 
no  microscopic  examination  has  been  made. 


CHAPTER  V. 

THE  LOWER  COAL  MEASURES,  OR  ALLEGHANY  RIVER  SERIES. 

THICKNESS,  CHARACTER,  AND  EXTENT. 

Below  the  Barren  Measures  or  Elk  River  series  there  occurs  a group 
of  rocks  (No.  XIII)  which  always  holds  valuable  coal  beds.  From  the 
fact  that  they  are  finely  exposed  along  the  Alleghany  River,  they  were 
long  ago  called  the  Alleghany  River  series,  and  their  geological  posi- 
tion in  the  general  scale  of  the  Carboniferous  gave  them  the  name 
Lower  Coal  Measures.  The  discovery  in  recent  years  that  the  next 
lower  group  of  beds  (the  Pottsville  Conglomerate)  sometimes  holds 
workable  coal,  has  been  used  as  an  argument  by  some  geologists  for 
breaking  up  the  old  nomenclature  and  rearranging  the  Carboniferous 
into  new  groups,  but  this  nomenclature  is  so  convenient,  and  expresses 
the  natural  divisions  of  the  rocks  so  well,  that  it  would  be  very  unwise 
to  make  any  such  changes  as  have  been  proposed,  since  it  would  be  of 
no  particular  service  and  would  only  bring  confusion  to  the  minds  of 
many  people  interested  in  Carboniferous  geology  who  are  now  thor- 
oughly conversant  with  the  old  and  tried  nomenclature  of  Pennsylvania 
and  Virginia.  Hence,  while  for  strictly  scientific  purposes  it  may  be 
well  to  group  the  Carboniferous  rocks  on  a wider  basis  as  proposed  in 
a former  part  of  this  report,  yet  for  every  day  field  work  in  practical 
geology,  the  old  nomenclature  can  not  be  improved  upon. 

The  Lower  Coal  Measures,  as  now  limited,  begin  at  the  top  with  the 
widely  distributed  and  valuable  Upper  Freeport  coal  bed  (a  horizon 
which  is  easily  recognized  anywhere  by  the  field  geologist)  and  extend 
down  through  several  beds  of  shale,  limestone,  coal,  and  sandstone  till 
a horizon  is  reached  where  a marked  change  in  lithology  takes  place, 
the  sandrocks  becoming  harder,  more  massive,  and  often  pebbly,  accom- 
panied with  a corresponding  change  in  the  character  of  the  imbedded 
fossils. 

The  thickness  of  this  series  varies  greatly  in  different  portions  of  the 
field,  beiug  not  far  from  300  feet  in  western  Pennsylvania,  and  seldom 
less  than  250  feet  anywhere  in  that  State,  except  in  the  Broad  Top 
field.  But  westward  through  Ohio  the  thickness  of  these  measures 
declines  until  around  the  northwestern  border  of  the  field  it  is  less  than 
200  feet.  Southward  from  this  region  of  Ohio,  where  the  Lower  Coal 
Measures  are  thinnest,  they  thickeu  up  rapidly  until  on  the  Great  Ka- 
nawha River  the  series  is  1,000  feet  thick,  and  the  same  on  the  Guyan- 

99 


100  THE  NORTHERN  BITUMINOUS  COAL  FIELD.  [bull.  65. 

dotte  and  Tug  Rivers.  Just  where  this  great  thickening  up  begins  in 
goingsouthwestward  from  the  Pennsylvania  line  is  not  exactly  known, 
but  there  are  good  reasons  for  believing  that  much  the  greater  portion 
of  it  takes  place  beyond  the  Little  Kanawha  River. 

The  topography  made  by  these  rocks  is  generally  very  much  the 
same,  except  where  the  thickness  is  very  great.  It  is  nearly  everywhere 
characterized  by  a hilly  country,  terraced  with  a series  of  parallel 
benches  which,  as  Lesley  long  ago  showed,  mark  the  outcrops  of  the 
several  coal  beds,  since  the  soft  rocks  usually  found  with  every  coal 
are  more  rapidly  eroded  than  the  harder  ones  above  or  below.  These 
coal  benches  are  not  confined  to  the  topography  of  the  Lower  Coal 
Measures,  since  they  are  due  to  a general  law  of  erosion,  but  are  only 
more  conspicuous  in  this  series  because  the  coal  beds  are  more  numer- 
ous and  closer  together. 

Through  Pennsylvania,  Ohio,  and  the  northern  half  of  West  Vir- 
ginia, with  few  exceptions,  the  hill  slopes  of  these  measures,  while  often 
rather  steep,  are  not  too  rugged  for  good  arable  and  grazing  lands,  and 
the  soils  are  usually  rich;  but  in  the  southwestern  part  of  West  Vir- 
ginia, where  these  rocks  have  increased  in  thickness  so  largely,  we  find 
a network  of  narrow  ridges,  generally  capped  with  the  Mahoning  sand- 
stone, from  which  the  surface  falls  away  at  an  angle  of  25°  to  40°  to 
the  beds  of  the  streams,  1,000  or  more  feet  below,  thus  practically  con- 
fining the  arable  land  to  the  narrow  valleys,  which  are  frequently 
trenched  into  the  top  members  of  the  next  underlying  or  Potts ville 
series  of  rocks. 

It  was  formerly  supposed  that  this  series  held  valuable  coal  only  in 
a broad  belt  around  the  margins  of  the  coal  field,  and  that  in  the  cen- 
ter of  the  Appalachian  basin,  where  these  beds  are  buried  under  1,500 
to  2.000  feet  of  superincumbent  strata,  they  contained  no  coals  thick 
enough  to  mine;  but  the  recent  drilling  of  many  oil  and  gas  wells  over 
the  central  portion  of  the  field  has  proved  the  supposition  to  be  un- 
founded, for  the  drill  has  many  times  j)enetrated  thick  beds  of  coal  in 
this  series  at  localities  where  they  underlie  the  surface  by  an  interval 
of  more  than  1,500  feet.  Hence,  aside  from  local  irregularities  always 
to  be  found  in  any  coal  field,  there  is  no  reason  for  believing  that  the 
Lower  Coal  Measures  do  not  contain  one  or  more  good  coal  beds  under 
nearly  every  portion  of  the  Appalachian  field,  and  where  it  would  seem 
to  be  otherwise  the  inference  has  been  founded  largely  on  defective 
records  of  borings,  in  which  no  attention  was  given  to  the  character  of 
the  beds  encountered  unless  they  proved  to  be  “ sands.”  But  while  it 
is  true  that  recent  drilling  has  shown  valuable  coal  in  this  series  along 
the  central  portion  of  the  trough  where  it  was  formerly  supposed  to  be 
absent,  yet  it  is  true  as  a general  law  that  the  coal  beds  of  this  series 
are  thicker  and  better  and  more  numerous  around  the  margins  of  the 
Appalachian  field  than  toward  the  center.  This  is  illustrated  by  the 


GEOLOGICAL  SURVE 


LOWER  COAL  MEASURES,  COALBURG,  KANAWHA  RIVER,  WEST  VIRGINIA. 


fBE  LIBRARY 
Of  THE 

UHSVERSITY  OF  ILLINOIS 


WHITE.]  THE  LOWER  COAL  MEASURES.  101 

distribution  of  the  Clarion  and  Brookville  beds,  which  are  valuable 
only  around  the  margin  of  the  coal  area. 

Owing  to  the  geological  position  of  the  Lower  Coal  Measures,  their 
beds  have  a much  wider  spread  and  are  accessible  over  a larger  area 
than  those  in  the  Upper  Coal  Measures,  so  that  when  in  the  distant 
future  the  upper  coals  and  the  easily  accessible  areas  of  the  lower  ones 
shall  have  been  exhausted,  there  will  still  remain  far  down  in  the 
trough  of  the  Appalachian  field  a great  wealth  of  fuel  which  can  be 
obtained  by  deep  shafting.  It  is  true  that  at  many  localities  disclosed 
by  the  drill  only  one  good  bed  of  coal  has  been  found  in  this  series 
where  it  lies  so  deep  beneath  the  surface,  but  that  is  also  true  of  the 
surface  outcrops,  and  many,  places  can  be  found  where  not  even  one 
good  coal  bed  occurs  in  the  surface  section,  and  many  others  where 
two  are  the  exception. 

The  main  strata  of  this  series,  which  have  been  recognized  and  traced 
over  a wide  area  in  the  three  States  with  which  this  report  deals,  have 
received  the  following  names  in  descending  order: 


Upper  Freeport  coal. 

Upper  Freeport  limestone. 
Upper  Freeport  sandstone. 
Lower  Freeport  coal. 

Lower  Freeport  limestone. 
Lower  Freeport  sandstone. 
Upper  Kittanning  coal. 
Johnstown  (Cement)  limestone. 
Middle  Kittanning  coal. 


Lower  Kittanning  coal. 
Lower  Kittanning  fire  clay. 
Lower  Kittanning  sandstone. 
Buhrstone  iron  ore. 
Ferriferous  limestone. 
Putnam  Hill  limestone. 
Clarion  coal. 

Brookville  coal. 


Other  beds  have  been  named  in  this  series  which  have  a local  dis- 
tribution, but  those  given  above  are  the  main  ones  which  can  be  traced 
and  identified  over  wide  areas. 

Prof.  Orton,  director  of  the  Ohio  Geological  Survey,  has  shown  that 
all  of  the  main  beds  of  the  Pennsylvania  Lower  Coal  Measures  can  be 
followed  and  identified  entirely  across  the  Ohio  coal  field  to  where  they 
enter  Kentucky ; and  the  writer  has  recently  shown  (The  Virgiuias, 
1885)  that  they  also  stretch  unbroken  around  the  southeastern  margin 
of  the  Appalachian  field,  from  the  Pennsylvania  line  down  through 
West  Virginia  to  the  Great  Kanawha,  and  on  across  the  Guyandotte 
to  the  Big  Sandy,  so  that  the  identifications  of  the  main  beds  of  coal, 
limestone,  and  sandstone  of  the  Lower  Coal  Measures  have  now  been 
carried  from  Pennsylvania  to  the  Kentucky  line,  on  both  sides  of  the 
Appalachian  field. 

As  illustrations  of  these  measures,  in  most  of  the  important  coal  re- 
gions of  the  area  in  question,  we  shall  now  present  a number  of  vertical 
sections.  The  identifications  of  the  several  beds  in  these  sections  have 
been  made  with  all  the  care  and  light  at  present  attainable,  and  while 
it  is  not  claimed  that  they  are  final  in  all  cases  and  free  from  error,  yet 
they  express  the  best  efforts  of  the  writer,  and  it  is  confidently  believed 


102 


THE  NORTHERN  BITUMINOUS  COAL  FIELD. 


[BULL.  65. 


that  their  publication  will  serve  to  stimulate  a more  careful  study  of 
the  general  stratigraphy  by  field  geologists  and  those  interested  in 
mining  enterprises,  so  that  finally  whatever  of  error  may  be  embodied 
in  these  identifications  will  be  discovered  and  eliminated.  It  is  certain 
that  the  first  effort  to  harmonize  the  stratigraphy  over  such  a large 
area  will  be  somewhat  provisional,  and  hence  the  writer  not  only  ex- 
pects, but  welcomes,  the  kindly  criticism  of  his  brother  geologists, 
knowing  that  all  will  be  pleased  when  the  true  order  and  succession  of 
these  beds  are  definitely  determined  in  the  several  important  regions 
of  the  Appalachian  field. 

In  some  cases,  like  that  at  Blossburg,  where  it  has  been  impossible 
to  identify  the  main  coal  beds  with  any  degree  of  certainty,  the  writer 
has  given  only  the  local  names  for  the  beds,  leaving  the  reader  to  draw 
his  own  conclusions  from  the  general  structure  of  the  section  5 but 
there  are  very  few  cases  where  some  one  of  the  seams  in  a given  section 
can  not  be  reasonably  determined. 

We  shall  begin  these  illustrations  of  the  Lower  Goal  Measures  at  the 
most  northern  point  of  the  Appalachian  Basin,  and  proceed  south- 
westward  through  the  field. 

Section  at  Blossburg , Pennsylvania . — The  structure  of  the  Lower  Coal 
Measures  at  the  northern  en$  of  the  Appalachian  basin  is  given  as 
follows  (Fig.  50)  for  the  Blossburg  region,  Tioga  County,  Pennsylvania, 
by  the  First  Geological  Survey  of  Pennsylvania,  Final  Report,  Yol.  II, 
page  520 : 

Blossburg , Tioga  County , Pennsylvania. 


■HiJgpWj 


r2TT~' ~ 


<*>• 

20' 

!?},oV 
uV 
3‘s" 

Fig.  50.— Section  at 
Blossburg,  Pa. 


2710 

aV-* 

30' 


47lo" 


[See  map,  B w.J 

Ft.  in.  Ft.  in. 

1.  Coal,  “Eock  vein” 3 6 

2.  Concealed T...  22 

3.  Coal,  “Seymour" 5 

4.  Slate  and  sandstone 10 

5.  Concealed  10  > 47  10 

6.  Sandstone,  pebbly,  with  thin  coal  near  top 27  10  ' 

7.  Coal,  “Dirty  vein” .iJi..  3 6 

8.  Slate  and  sandstone 30 

9.  Coal. 1 6 

10.  Fireclay 3 

11.  Slate 20 

( Coal 3'  6”  ) 

12.  Coal,  “Bloss  vein”.  < Fire  clay. 5'  0"  > 10  6 

( Coal 2'  V'S 

13.  Argillaceous  sandstone,  with  two  thin  coals 13  6 

14.  Coal,  “ Bear  Creek  ” 3 6 

15.  Sandstone. 

163  10 


Total. 


The  “ Bloss  vein”  seems  to  be  identical  with  the  Lower  Kittanning 


bed  of  the  Alleghany  River,  while  the  “Rock  vein”  and  “Seymour” 
are  possibly  identical  with  the  Upper  and  Lower  Freeport  beds,  respect- 
ively. This  would  make  Nos.  7 and  9 the  Upper  and  Middle  Kittan- 
ning. 


WHITE.] 


THE  LOWER  COAL  MEASURES. 


103 


Section  at  Fall  Brook , Pennsylvania. — At  Fall  Brook,  8 miles  north- 
east from  Blossburg,  and  the  most  northern  development  in  the  Appala- 
chian coal  field,  the  structure  of  the  Lower  Coal  Measures  is  given  as 
follows  (Fig.  51)  by  Mr.  Franklin  Platt,  in  Beport  G,  pages  166,  169, 
Second  Geological  Survey  of  Pennsylvania : 

Fall  Brook,  Tioga  County,  Pennsylvania. 


[See  map,  B x.] 


Ft.  in. 

2 6 


1.  Coal,  “Seymour” 

2.  Bough,  sandy  fire  clay 2 

3.  Sandstone,  massive,  pebbly 50 


Coal. 


4.  Coal < Sandstone,  thin  bedded 

( Coal 

5.  Eire  clay 

6.  Sandstone 

7.  Slate 

[Coal.. 

Slate . 

Dirty  vein  ” { Coal. 


1'  8" 
3'  0" 
O'  7" 


8.  Coal, 


mp 

Fig.  51. — Section 
at  Fall  Brook , 
Pa. 


1'  3"  ] 

4'  0"  | 

, 1'  2"  > 

Slate  . 0'  3"  | 

[Coal..  0'  10" ) 

9.  Bough,  hard  fire  clay , 2 

10.  Gray  shaly  rock  20 

11.  Fire  clay,  with  kidney  ore  at  bottom - 2 

12.  Sandstone,  light  gray 9 

13.  Clay  slate 5 

14.  Coal,  “Bloss  vein” 4 

15.  Fire  clay,  pure 3 

16.  Sandy  slate,  some  sandy  layers 16 

17.  Coal  and  slate,  “ Bear  Creek  ” 1 

18.  Sandy  clay 4 

19.  Sandstone. 


Total 


146 


Section  near  Karthaus,  Pennsylvania. — About  65  miles  southwest  of 
Blossburg,  in  the  northeastern  corner  of  Clearfield  County,  Penn- 
sylvania, the  following  section  (Fig.  52)  of  the  Lower  Coal  Measures 
is  reported  from  the  vicinity  of  Karthaus,  by  H.  D.  Kogers,  in  the  First 
Geological  Survey  of  Pennsylvania : 


near  Karthaus, 
Pa. 


Karthaus,  Clearfield  County,  Pennsylvania. 

[See  map,  E t.] 

Coal,  Upper  Freeport 

Fire  clay 

Sandstone,  brown 

Coal 

Fire  clay 

Limestone,  siliceous 

Shale 

Sandstone,  brown 

Coal,  Lower  Freeport 

Slate  

Sandstone,  gray,  Freeport 

Coal,  Upper  Kittanniug 

Shale,  containing  iron  ore 

Coal.  Middle  Kittanning 

Sandstone  and  slate 

( Coal. 1'  0"l 

Coal,  Lower  Kittanning < Slate O'  3"  > 

(Coal 2'  6"  ) 

Fire  clay 

Sandstone,  brown 

Coal,  Clarion 

Fire  clay,  ferruginous 

Shales,  containing  iron  ore  band 

Shales  and  slates 

Coal,  Brookville 

No.  XII  Conglomerate. 

Total 


Ft.  in. 
6 

2 6 
45 

0 ie 
2 

3 6 

1 

26 

3 

1 6 
37 

3 2 

11 
1 

21 

3 9 

2 6 
35 

1 6 

3 

11  9 

22 
1 


245 


104 


THE  NORTHERN  BITUMINOUS  COAL  FIELD. 


Tbull.  65. 


Section  in  Horton  Township,  Hlk  County , Pennsylvania. — Horton  Town- 
ship, Elk  County,  Pennsylvania,  lies  on  the  borders  of  Clearfield  and 
Jefferson  Counties,  30  miles  west  from  Karthaus  and 
about  80  miles  distant  west-southwest  from  the  Bloss- 
burg  region.  In  this  township  Mr.  C.  A.  Ashburner 
finds  the  following  section  (Fig.  53)  for  the  Lower  Coal 
Measures,  Eeport  BE,  page  227 : 

Horton  Township,  Elk  County,  Pennsylvania. 

[See  map,  Dq.j 


Fig.  53. — Section  in 
Elk  County,  Pa. 


( Coal 3 

1.  Coal,  Upper  Freeport n Fire  clay  and  shale. . . 10 

( Coal 3 

2.  Fire  clay  and  sandstone 

3.  Limestone,  Upper  Freeport 

4.  Slaty  sandstone 

5.  Coal,  Middle  Freeport 

6.  Soft  gray  slates 

t Cannel 2' 

7.  Coal,  Lower  Freeport < Slate 16' 

( Coal 3' 

8.  Sandstone - 

9.  Limestone.  Lower  Freeport 

10.  Flaggy  sandstone  and  slates 

11.  Coal,  Upper  Kittanning 

12.  Fire  clay  and  slate 

13.  Limestone,  Johnstown  Cement 

14.  Concealed 

35.  Coal,  Middle  Kittanning 

16.  Black  slate  

17.  Coal,  Lower  Kittanning 

18.  Shale  and  sandstone,  occasional  coal  streak 

19.  Limestone,  Ferriferous 

20.  Shale  and  slate 

21.  Coal,  Clarion 

22.  Massive  sandstone,  top  of  XU. 

Total 


Feet. 

16 


:!■ 


327 


Section  near  Broclcwayville , Pennsylvania . — Snyder  Township,  Jeffer- 
son County,  adjoins  Horton,  and  there,  near  Brockwayville,  Mr.  Wm. 

G.  Platt  reports  the  following  structure  (Fig.  54)  for  the 
Lower  Coal  Measures,  Eeport  H6,  pages  186, 187 : 


2V 


Fig.  54. — Section 
near  Brockway- 
ville, Pa. 


Brockwayville,  Jefferson  County,  Pennsylvania. 

[See  map,  D q.] 

Ft.  in. 

1.  Coal,  Upper  Freeport ~ 3 

2.  Clay,  impure 3 

3.  Limestone,  Upper  Freeport 5 

4.  Concealed 24 

5.  Sandstone,  thin-bedded 5 

6.  Shales  and  slates 6 

7.  Coal,  Lower  Freeport ' 3 6 

8.  Clay,  impure 5 

9.  Limestone,  Lower  Freeport 2 6 

10.  Concealed 18 

12.  Sandstone 15 

13.  Slates 5 

14.  Coal,  Upper  Kittanning 3 6 

35.  Clay  shales 12 

16.  Limestone,  Johnstown  Cement 2 

17.  Concealed,  shales  (?) 40 

38.  Coal,  Middle  Kittanning 2 

19.  Concealed,  sandstone  at  base 45 

20.  Coal,  Lower  Kittanning 2 1 6 

21.  Shales 35 

22.  Iron  ore,  Buhrstone 6 

23.  Limestone,  Ferriferous 5 

24.  Sandstone  and  shales 20 

25.  Concealed 15 

26.  Coal,  Clarion 3 

27.  Shales 10 

28.  Sandstone,  massive,  top  of  XII. 


Total 


290 


WHITE.! 


THE  LOWER  COAL  MEASURES. 


105 


Section  in  Clarion  County , Pennsylvania. — Clarion  County  lies  next 
west  from  Jefferson,  and  Mr.  H.  Martyn  Chance  gives  in  Report  VV", 
page  32,  Second  Geological  Survey  of  Pennsylvania,  the 
following  as  the  general  structure  of  the  Lower  Coal 
Measures  in  that  county  (Fig.  55) : 


Fig.  55. — Section 

in  Clarion  Co., 


Clarion  County,  Pennsylvania. 


[See  map,  E o.J 

1.  Coal,  Upper  Freeport 

2.  Fireclay. 

3.  Limestone,  Upper  Freeport 

4.  Sliale,  with  ore 

5.  Sandstone 

6.  Shale 

7.  Coal,  Lower  Freeport 

8.  Fire  clay 

9.  Limestone,  Lower  Freeport 

10.  Sandstone  and  shales 

11.  Shale 

12.  Coal,  Upper  Kittanning 

13.  Fire  clay  or  shale 

14.  Limestone,  Johnstown  Cement  bed 

15.  Shalv  measures 

16.  Coalj  Middle  Kittanning 

17.  Fireclay 

18.  Shale  and  sandstone 

19.  Coal,  Lower  Kittanning 

20.  Sandstone  and  shale,  with  ore 

21.  Ore,  Buhrstone 

22.  Limestone,  Ferriferous 

23.  Shale 

C Coal . . . ..I  2' ) 

24.  Clarion  coal < Slaty  sbalo. ....  25'  > 

( Coai y..  3L> 

25.  Fireclay 

26.  Shale  and  sandstone 

27.  Coal,  Brookville 

28.  Fire  clay 

29.  Massive  sandstone,  XII. 


Ft 


Pa. 


Total - 335 


* Section  at  Miller's  Eddy,  Clarion  County , Pennsylvania . — 
zsryr  The  following  section  (Fig.  56),  made  by  Mr.  John  Hag- 

* gerty,  M.  E.,  of  Brady’s  Bend,  Pennsylvania,  represents 
the  Lower  Coal  Measure  structure  at  Miller’s  Eddy,  near 
the  mouth  of  the  Clarion  River  (YV,  p.  123) : 


to/ 


IB'S- 


Miller's  Eddy , Clarion  County,  Pennsylvania. 

[See  map,  En.] 


2.  Interval. 

3.  Iron  ore. 


6.  Interval . . . 

7.  Sandstone. 


9.  Coal,  Lower  Kittanning. 
10.  Interval 


12.  Limestone,  Ferriferous. 

13.  Shales 

14.  Sandstone 


Fig.  56. — Section 
at  Miller’s  Eddy, 

Pa. 


16.  Blue  shales 

17.  Sandstone,  massive. 


Total 312 


Ft.  in. 

3 

28 

3 

2 

103 

1 

6 

20 

30 

16 

6 

3 

6 

10 

19 

10 

9 

6 

28 

6 

2 

4 

29 

312 

5 

106 


THE  NORTHERN  BITUMINOUS  COAL  FIELD. 


[BULL.  65. 


Section  at  East  Brady , Clarion  County , Pennsylvania . — Mr.  Haggerty 
also  leveled  another  section  of  these  measures  at  East  Brady,  in  the 
southwestern  corner  of  Clarion  County,  which  is  given  as 
follows  (Fig.  57)  in  Report  YV,  p.  77 : 

East  Brady , Clarion  County , Pennsylvania . 


[See  map,  F n.] 

Ft.  in. 

Coal.  Upper  Freeport 2 

Concealed  and  sandstone -. 108 

Coal,  Upper  Kittanning 1 5 

Sandstone 9 

Interval 57  0 

Coal,  Lower  Kittanning 3 6 

Shale,  with  sandstone 40  6 

Limestone,  Ferriferous 10 

Interval 22  2 


Coal,  Clarion 

Sandstone 

Coal,  thin,  Brookville. 
Sandstone,  No.  XII. 


Fig.  57. — Section 
at  East  Brady, 


Total. 


279 


Section  near  New  Bethlehem , Pennsylvania . — Mr.  Chance  gives  the 
following  (Fig.  58)  as  the  structure  of  the  Lower  Coal  Measures  in  the 
vicinity  of  New  Bethlehem,  on  the  Red  Bank  River,  in 
southeastern  Clarion  County,  YY,  p.  88 : 


Fig.  58.— Section 
near  New  Beth- 
lehem, Pa. 


Near  New  Bethlehem,  Clarion  County,  Pennsylvania . 

[See  map,  F o.] 

1.  Coal,  Upper  Freeport 

2.  Fireclay 

3.  Sandy  shale  and  sandstone 

4.  Coal,  Lower  Freeport - 

5.  Fire  clay 

6.  Concealed,  sandstone,  and  shale 

7.  Coal,  Upper  Kittanning  

8.  Fire  clay 

9.  Shale 

10.  Coal,  Middle  Kittanning  (?) 

11.  Fire  clay 

12.  Concealed 

13.  Ore,  Buhrstone 

14.  Limestone,  Ferriferous 

15.  Concealed 

16.  Sandstone,  top  of  XII. 


Ft. 

5 

3 

42 
7 
3 

65 

3 

4 

43 
2 

3 

60 

1 

4 

50 


Total 295 


WHITE.) 


THE  LOWER  COAL  MEASURES. 


107 


Section  in  Brady  Township , Butler  County , Pennsylvania. — In  the 
northwestern  portion  of  Butler  County  (Brady  Township),  Mr.  Chance 
gives,  in  Beport  V,  the  following  section  (Fig.  59)  for 
the  Lower  Coal  Measures  down  to  and  including  the 
Ferriferous  limestone,  and  the  portion  below  that  is 
added  from  an  exposure  in  an  adjoining  township : 


60’ 


Brady  Township,  Butler  County. 

[See  map,  F L] 


Ft.  Ft. 


55' 


1.  Coal,  Upper  Freeport 

2.  Fire  clay 

3.  Shale  and  sandstone 

4.  Coal,  Lower  Freeport 

5.  Concealed,  and  massive  sandstone 

6.  Massive  sandstone 

7.  Coal,  Upper  Kittanning 

8.  Concealed,  and  shale 

9.  Coal,  Middle  Kittanning  (?) 

10.  Concealed 

11.  Iron  ore thin  l 

12.  Concealed -• 55  j 

13.  Limestone,  Ferriferous 

14.  Coal,  Scrubgrass 

15.  Shales 

1G.  Coal,  Brookville 


m. 

G 


45, 

15  i 


10) 


Total 


GO 


3 

55 

3 

65 

15 

1 


328 


Section  near  Ore  Hill  Furnace , Armstrong  County , 

fig.  59. Section  in  But-  Pennsylvania. — In  the  vicinity  of  Ore  Hill  Furnace, 

ier  county,  Pa.  Armstrong  County,  Pennsylvania,  3 miles  below  the 
mouth  of  the  Mahoning  Fiver,  the  writer  found  the  fol- 
( lowing  succession  (Fig.  60) : 


Ore  Hill  Furnace,  Armstrong  County,  Pennsylvania. 


[See  map,  G o.] 

1.  Coal,  Upper  Freeport 

2.  Fire  clay  with  iron  ore 

3.  Flaggy  sandstone  and  shales 

4.  Bit  uminous  shales 

5.  Coal,  blossom.  Lower  Freeport 

6.  Fire  clay  and  limestones,  Lower  Freeport 

7.  Flaggy  sandstone  and  dark  shales 

8.  Limestone,  gray,  Johnstown  Cement 

9.  Concealed  and  sandstone 

10.  Coal,  Middle  Kittanning 

11.  Fire  clay 

12.  Sandy  shale 

(Coal V 0' 

13.  Coal,  Lower  Kittanning  (Shale 4'  0" 

( Coal O'  6" 

14.  Fire  clay 

15.  Shales,  brown,  sandy 

16.  Iron  ore,  Buhrstone 

17.  Limestone,  Ferriferous 

Fig.  60.— Section  near  18.  Concealed  and  shales  to  top  of  No.  XII  sandstone  in  Al- 

Ore  Hill  Furnace*  leghany  River 


Ft. 

Ft.  in. 

2 6 

8) 

20  V 

33 

5) 

30  \ 

35 

1 

50 

J"  s 


Armstrong  County* 

Pa. 


Total 


247 


This  section  exhibits  a rapid  thinning  away  of  the  whole  column, 
but  principally  in  that  part  of  it  between  the  Upper  Freeport  and  the 
Upper  Kittanning  coals. 


108 


THE  NORTHERN  BITUMINOUS  COAL  FIELD. 


[BULL.  65. 


Section  near  Centerville , Pennsylvania. — Five  miles  northeast  from  Ore 
Hill  Furnace,  the  following  succession  (Fig.  61)  is  reported  from  the 
vicinity  of  Centerville  by  Mr.  Win.  G.  Platt,  in  Eeport 
H5,  Second  Geological  Survey  of  Pennsylvania,  pages 


163, 164. 


Centerville , Armstrong  County,  Pennsylvania. 

[See  map,  G-  o.J 


Ft. 


15  ) 


65 


Fig.  61.— Section 

near  Centerville, 
Pa. 


1.  Coal,  Upper  Freeport 

2.  Clay  shales,  with  iron  ore 

3.  Limestone,  Freeport u > 

4.  Concealed  15  ) 

5.  Coal,  Lower  Freeport : . . . 

6.  Concealed  

7.  Iron  ore,  siliceous 

8.  Sandstone 

9.  Coal,  blossom 

10.  Concealed 

11.  Coal,  Upper  Kittanning 

12.  Concealed 

13.  Coal,  Middle  Kittanning 

14.  Concealed 

15.  Iron  ore,  Buhrstone 

16.  Limestone,  Ferriferous 

17.  Concealed 

18.  Cannel  slate  (Clarion  coal) .. 

19.  Concealed 

20.  Black  slate  (Brookville  coal). 

21.  Top  of  No.  XII  conglomerate. 

Total 298  2 

Section  at  Putnfyville,  Pennsylvania. — Five  miles  east 
of  Centerville  is  the  village  of  Putney  ville,  and  from 
this  vicinity  Mr.  Wm.  G.  Platt  reports  the  following 


Ft. 

in. 

3 

10 

35 

3 

6 

37 

46 

1 

27 

1 

6 

65 

0 

4 

8 

30 

40 

298 

2 

section  (Fig.  62)  of  the  series  H5,  p.  150: 


rtf 


42 r 


SX* 


Putneyville,  Armstrong  County,  Pennsylvania, 

[See  map,  G o.] 

1.  Coal.  Upper  Freeport 


6.  Coal,  Lower  Freeport 

7.  Slate 


10.  Concealed 


12.  Coal,  blossom,  Upper  Kittanning  . . . 

13.  Limestone,  Johnstown  Cement  bed. 

14.  Clay 


17.  Coal,  Middle  Kittanning 

18.  Concealed 

19.  Slates,  with  sandstone  layers. 

20.  Coal,  Lower  Kittanning 

21.  Fire  clay,  impure 


24.  Limestone, Ferriferous 

25.  Sandstone,  flaggy 

26.  Black  slates 

27.  Cannel  slate  (Clarion  coal) 

28.  Concealed  

29.  Brookville  coal. 

30.  Top  of  No.  XII,  conglomerate. 


Ft.  in. 

Ft. 

in. 

4 

G 

12 

) 

5 

10 

1 

> 

j 

42 

15 

3 

1 

6 

[ 

0 

3 

2 

53 

9 

30 

20 

J 

4 

3 

15 

58 

40 

> 

1 

8 

30 

20 

} 

50 

2 

6 

J 

20 

5 

26 

4 

0 

4 

5 

Fig.  62. — Section  at 
Putneyville,  Pa. 


Total 


314  3 


t«.y- 


WHITE.} 


THE  LOWER  COAL  MEASURES. 


109 


Section  near  Kittanning , Pennsylvania. — In  the  vicinity  of  Kittan- 
ning, Pennsylvania,  the  succession  of  the  Lower  Coal  Measures  is  as 
follows  (Fig.  63) : 

Vicinity  of  Kittanning,  Pennsylvania. 


[See  map,  G n.j 

Ft.  in. 

1.  Coal,  Upper  Freeport 

2.  Shales,  and  concealed 

3.  Coal,  Lower  Freeport 

4.  Concealed,  and  massive  sandstone 35 

5.  Shales  and  sandstone 40 

6.  Coal,  slate  in  center.  Middle  Kittanning 

7.  Fire  clay 4 

8.  Sandy  shales 6 

9.  Fire  clay 3 

10.  Flaggy  sandstone 17 


11.  Shales,  dark,  sandy,  with  iron  ore. 

('Coal... 
i Slate  . . 

12.  Coal,  Lower  Kittanning . . ^ Coal . . . 


40 


1' 

10"  } 

O' 

2"  | 

0' 

8"  > 

.0' 

1"  1 

.0' 

6"J 

L Coal 

13.  Fire  clay  - 5 

14.  Sandstone  and  sandy  shales 

15.  Shales,  with  iron  ore  

16.  Iron  ore,  Buhrstone 

17.  Limestone,  Ferriferous 11 

18.  Sandy  shales 15 

19.  Coal 

20.  Sandy  shales  and  sandstone 

21.  Coal,  Clarion 

22.  Concealed,  to  top  of  Xo.  XII  sandstone 


Ft.  in. 

4 

35 

2 

75 

1 6 


Fig.  63. — Section  near 
Kittanning,  Pa. 


Total . 


D 

40 

} 

> 50 

5 

► 

0 

6 > 

11 

6 

> 27 

15 

0 

21 

1 

25 

315 

Section  5 miles  south  of  Kittanning,  Pennsylvania. — About  5 miles 
south  of  Kittanning  and  1 mile  below  the  mouth  of  Crooked  Creek  a 
very  important  exposure  may  be  seen  on  the  left  bluff  of  the  Allegheny 
Eiver,  since  it  gives  in  a clear  manner  the  relations  of  the  upper  mem- 
bers of  the  Lower  Coal  Measures.  The  section  there  (Fig.  64)  was 
carefully  leveled  by  the  writer,  and  reads  as  follows : 


Five  miles  helow  Kittanning. 


[See  map,  G n.  ] 

1.  Coal,  Upper  Freeport,  blossom 

2.  Fireclay 

3.  Sandstone 

4.  Fire  clay  and  shales 

5.  Concealed  . 

6.  Limestone,  Upper  Freeport 

7.  Concealed 

8.  Shales,  bluish 

t Coal  ....  0'  2"  I 

9.  Coal,  Lb wer  Freeport. ..  < Slate r 8"  t 

t Coal 1'  8") 

10.  Fire  clay  and  shales - 

11.  Sandstone,  massivo,  pebbly,  Frbepmt 

12.  Coal,  Upper  Kit lunn in g .->.;!■> 

13.  Shales,  daik 

14.  Coal,  slate  in  center,  Middle  Kittanuing 

15.  Limestone,  sandy 

16.  Fire  clay 

17.  Sandstone,  flaggy 

18.  Fireclay 

19.  Sandstone,  flaggy 

20.  Shales,  dark 


Ft.  in. 


2 6) 
2 6 

5 

10 

35 

20 


10 

45 


Ft.  in. 


80 


3 6 


55 

0 6 
20 

1 6 
1 6 

3 

3 - 

5 
8 
10 


Total 


191 


110 


THE  NORTHERN  BITUMINOUS  COAL  FIELD. 


[BULL.  65. 


Section  at  Logansport , Pennsylvania , — The  last  section  gets  its  special 
significance  when  compared  with  another  one,  obtained  2 miles  below, 
on  the  right  bank  of  the  Alleghany  River,  and  opposite  the  town  of 
Logansport.  The  section  there  (Fig.  65)  gives  the  following  structure; 

Logansport,  Armstrong  County,  Pennsylvania. 


[See  map,  Gr  n.] 


Ft. 


1.  Coal,  Upper  Freeport. 

2.  Fire  clay 


f Impure  limestone. 2' ) 

I Limy  shales 4' 

I Limestone,  good V 

3.  Limestone,  Upper  Freeport Shales V 

I Limestone,  “glassy  layer” 2' 

, Limy  shales 2' 

[ Limestone,  good 2' 


70 


51’ 


Fig.  65. — Section  at  Lo- 
gansport, Pa. 


' 8” ) 

' 2"L. 
' 6”  ) 


f Coal 

V 

1" 

j Slate 

l" 

17.  Coal,  Lower  Kittanning . . <{  Coal 

V 

1" 

| Slate 

0' 

V 

1 Coal 

V 

2" 

Ft.  in. 
3 


4) 


14  )•  28 


18.  Concealed  to  river  level 

19.  To  base  of  Lower  Coal  Measures,  about 


4.  Shales  and  fire  clay 10  J 

fCoal 2'  0”) 

5.  Coal,  Lower  Freeport < Fire  clay,  impure.  2'  4''  > .. 

( Coal 4'  8"  ) 

6.  Concealed 11  » 

7.  Very  massive,  grayish  white,  pebbly  sandstone,  Freeport  70  > 

8.  Coal,  ltl>per  Kittanning. ...L.  ...;v 

9.  Dark  gray  shales v 

( Coal  0 

10.  Coal,  Middle  Kittanning.  \ Slate 0 

, f Coal 0 

11.  Fireclay ?.* 

12.  Limestone  

13.  Fire  clay,  with  limestone  nodules  in  top . 

14.  Sandstone,  shaly 

15.  Concealed  (shales) 1 

16.  Blue  shales  


7 

15 
20  J 


81 

0 8 
20 

1 4 


y 52 


3 6 


Total 298  6 


Here  we  find  a ferruginous  limestone  making  its  appearance  under 
what  the  section  shows  to  be  the  Middle  Kittanuing  coal,  and  it  is  pos- 
sible that  this  same  bed  may  have  occasionally  been  identified  with 
the  Johnstown  Cement  limestone  in  this  portion  of  Pennsylvania, 
which  would  be  erroneous,  since  that  bed  belongs  under  the  little  coal, 
No.  8 of  the  section,  while  the  Johnstown  Cement  bed,  as  correlated  by 
Messrs.  Platt  and  others,  comes  just  under  the  Upper  Kittanuing  coal. 

The  section  also  exhibits  the  great  variations  that  may  take  place 
in  the  thickness  of  the  intervals  between  important  coal  beds,  that 
between  the  two  Freeports  being  here  reduced  to  only  28  feet. 


WHITE.] 


THE  LOWER  COAL  MEASURES. 


Ill 


Section  at  Freeport,  Pennsylvania . — Freeport,  on  the  Alleghany  River, 
at  the  southern  point  of  Armstrong  County  and  7 miles  southwest  of 
Logansport,  is  a classic  locality  for  the  upper  portion  of  the  Lower  Coal 
Measures,  and  the  following  section  (Fig.  66),  taken  there,  is  given 
for  the  purpose  of  illustrating  the  relations  of  the  Upper  and  Lower 
Freeport  coals  at  this  typical  locality : 


Freeport , Pennsylvania. 
[See  map,  G n.] 


Ft.  in. 


[Coal 2'  8 "l 

1 Slate,  gray O'  1^"  ( 

1.  Coal,  Upper  Freeport  { Coal O'  J> 

1 Slate,  dark  gray 0?  0-£"  i 

( Coal,  sulphurous O'  5 " J 

2.  Fire  clay 


3.  Limestone,  Upper  Freeport 3 

4.  Sandy  shales 20 

5.  Coal,  Middle  Freeport . . Jr.C V'-i 2 

6.  Sandy  shales  and  sandstone 39 

[ Cannel  slate...  5'  0"] 

^ j Slaty  coal 4' 


7.  Coal,  Lower  Froeport  <J  Fire  clay  with  } 

^ " | limestone 2'  6"  | 

(Slaty  coal 2'  6"j 

8.  Fire  clay  and  shales 2 


g ! 


Fig.  66.— Section  at 
Freeport,  Pa. 


g-2  ^ 10.  Coaly  slate,  Upper  Kittannin 
jr§  (11.  Sandstone,  gray,  massive 15 

12.  Coal,  Middle  Kittanning 

13.  Fire  clay,  with  limestonenodules in  upper  half.. 

Total 


Ft.  in. 
3 


14 


64 


155  3J 


This  section  shows  that  there  is  a third  Freeport  coal,  coming  nearly 
midway  between  the  upper  and  lower  ones,  at  this,  their  typical 
locality,  a fact  that  has  been  frequently  overlooked  by  geologists,  and 
that  has  led  to  error  in  identifications.  This  Middle  Freeport  coal,  as 

I have  termed  it,  is  not  persistent;  but  the  fact  that  there  is  such  a 
bed  in  the  series  occasionally  should  lead  to  careful  scrutiny  of  this 
portion  of  the  column  of  rocks  before  positive  identification  of  the 
Lower  Freeport  coal. 

This  latter  bed,  No.  7,  also  has  elements  of  possible  confusion  in  its 
structure  here  at  its  type  locality,  since,  as  may  be  seen  from  the  sec- 
tion, it  is  a double  bed,  made  so  by  2J  feet  of  fire  clay,  in  which  a nod- 
ular limestone  occurs.  It  is  possible  that  these  parting  rocks  may 
expand  to  several  feet  in  some  regions,  and  thus  give  two  Lower 
Freeport  coals,  as  indeed  they  are  known  to  do. 

I have  included  No.  11  as  a part  of  the  Freeport  sandstone,  since  at 
one  locality  the  coal  bed  No.  10  thins  out  entirely  and  lets  Nos.  9 and 

II  unite  into  one  solid  sandstone;  but  it  is  possible  that  No.  9 alone 
should  be  included  under  the  name  Freeport  sandstone,  as  originally 
intended  by  Rogers. 


112 


THE  NORTHERN  BIT  OMINOUS  COAL  FIELD, 


[BULL.  65, 


Section  near  mouth  of  Beaver  River , Pennsylvania.  —In  the  region 
about  the  month  of  the  Beaver  River,  the  Lower  Goal 
Measures  thicken  up  to  a considerable  extent,  through 
the  local  expansion  of  some  members,  as  shown  by 
the  following  (Fig.  67)  section  of  the  structure  there: 


vX\\\%%vJv:  tst 


4d 


Near  mouth  of  Beaver  River , Beaver  County,  Pennsylvania. 


87' 


iiifliiiililiN 


42' 


80' 


i81f 


[See  map,  Gk.] 

Ft. 

1.  Coal,  Upper  Freeport 

2.  Fireclay... 4 

3.  Limestone,  Upper  Freeport i 2 

4.  Shales,  sandy 55 

5.  Coal,  Lower  Freeport 1 

6.  Shales,  sandy 12 

7.  Sandstone,  massive,  Freeport 75 

8.  Coal,  Middle  Kittanning 

9.  Fire  clay  3 

10.  Shales,  sandy,  dark 40 

11.  Coal,  Lower  Kittanning ®i 

12.  Fire  clay : 8 

13.  Sandstone,  flaggy  and  massive 42 

14.  Shales,  sandy  . . 1 r 30 

15.  Limestone,  Ferriferous  

16.  Black  fossiliferous  shales 12 

17.  Fireclay 8 

18.  Sandy  shales 10 

19.  Fire  clay,  non-plastic 3 

20.  Sandstone,  flaggy 23 

21.  Shales,  sandy  25 

22.  Coal,  Brookville 

23.  Fire  clay 

24.  Massive  sandstone,  No.  XII. 


Ft.  in. 
3 


61 


81 


Total 


369 


Section  at  Sewicldey , Pennsylvania. — At  Sewickley, 
Alleghany  County,  Pennsylvania,  a test  hole  for  coal 
F moutiT of CB°ena vG© r was  bored  by  Mr.  Cochran  Fleming,  through  whose 
Kiver, Pa.  courtesy  the  writer  had  the  opportunity  of  measuring 

the  carefully  preserved  cores  from  the  diamond  drill,  which  gave  this 
structure  (Fig.  68)  for  the  rocks  of  the  Lower  Coal 
Measures  there : 


a 


nil 
His 


Sewickley,  Alleghany  County,  Pennsylvania. 

[See  map,  H 1.] 

Ft.  in. 


7S* 


Fjg.  68.— Section  at  Se 
wiekley,  Fa, 


1.  Coal,  Upper  Freeport 

2.  Fire  clay  15 

3.  Shales,  blue,  sandy 9 

4.  Sandstone 0 

5.  Fireclay 3 

6.  Sandstone 1 

7.  Shales 16 

8.  Dark  slate 6 

9.  Coal,  slaty,  Lower  Freeport  

10.  Fire  clay,  good 1 

11.  Fire  clay,  sandy  3 

12.  Gray,  micaceous  sandstone  $ °n6  "•*«/  <u// 

in  thin  layers  Freeport \^dstobe % 

13.  Coal,  Upper  Kittanuing 

14.  Sandstone 16 

15.  tire  clay  (Middle  Kittanning  coal  horizon) 8 

16.  Shales,  dark,  in terst ratified  with  fire  clav  48 

( Coal ..1'  4' 

17.  Coal,  Lower  Kittanning < Slate 0'  1 

(Coal 0 

18.  Fire  clay,  good 

19.  Shales,  blue 

20.  Interval  to  top  of  No.  XII,  estimated 


Ft.  in. 


L 


i 

39  6J  f 


Total . 


l 3 

44  Si 

0 4i 

73 


8 

16  10 
75 

£75  8 


WHITE.  J 


THE  LOWER  COAL  MEASURES. 


113 


Section  at  Washington , Pennsylvania. — At  Washington,  Pennsylvania, 
the  top  of  this  series  is  1,000  feet  below  the  surface,  and  Prof.  Linton, 
of  Washington  and  Jefferson  College,  gives  the  follow- 
ing (Fig.  69)  as  the  structure  of  its  rocks  according 
to  the  record  of  the  Thayer  oil  well,  the  drillings  from 
which  he  very  carefully  studied  (Geological  Survey  of 
Pennsylvania,  1886,  pp.  764,  765) : 


Under  Washington,  Pennsylvania. 

fSee  map,  J k.] 

1.  Upner  Freeport  coal— absent 

2.  Dark  shale  with  limestone  at  bottom,  Upper  Freeport 

3.  Sandstone,  dark 

4.  Sandstone,  white 

5.  Sandstone,  dark,  with  limestone 

6.  Sandstone, hard 

7.  Shale,  dark 

8.  Shale,  variegated  with  dark  lime 

9.  Limestone,  Johnstown  Cement  - - ^ fight’  * g/j 

10.  Shale,  dark,  slaty 

11.  Shale  and  coal,  Middle  Kittanning 

12.  Shale,  slate  and  shells 

13.  Sandstone,  grayish 

14.  Shale,  gray 

15.  Sandstone,  grayish,  shaly 

16.  Shale  and  shells 


Total 


Ft. 

Ft. 

12  ) 

36  > 

64 

16  S 

4 

19  ) 

28  > 

55 

8 > 

11 

30 

30  ] 
26  [ 

6 

U > 

115 

29  | 

19  J 

285 

it  would 

Fig  69.— Section  under 
Washington,  Pa. 

Here  there  is  only  one  coal  present  in  the  series  and 
appear  to  be  the  Middle  Kittanning. 

Section  near  Carpenters  Station , W estmor eland  County , Pennsylvania. — 
Kear  the  main  line  of  the  Pennsylvania  Eailroad,  in  the  vicinity  of  Car- 
penter’s Station,  Westmoreland  County,  Pennsylvania,  a 
well  was  drilled  for  gas  by  Mr.  E.  M.  Hukill,  who  thus 
(Fig.  70)  reports  the  structure  of  the  Lower  Coal  Meas- 
ures, as  published  in  Geological  Survey  of  Pennsylvania, 
1886,  p.  726: 


|»r 

i 

44  6 


Near  Carpenter’s  Station , Westmoreland  County,  Pennsylvania. 

[See  map,  In.] 


7.  Sandstone,  Freeport 


1.  Coal,  Upper  Freeport 

2.  Fireclay  (shales) 

3.  Coal,  Lower  Freeport 

4.  Fire  clay 

5.  Sandstone,  gray 

6.  Slate 

C Sandstono,  hard . 
< Sandstone,  soft  . 
( Sandstone,  hard. 

8.  Slate 

9.  Sandstono 

10.  Slate  and  shells 

11.  Slate,  black 

18.  Coal,  Clarion  or  Lower  Kittanning 

19.  Fire  clay 

20.  Shale  and  shells 

70.— Section  21.  Sandstone,  top  of  XII. 


6 ') 
44' [ 
13' > 


Fig. 

near  Canjen  ter’s 
Station,  Pa. 


Total 

Bull.  65 


Ft. 

Ft. 

2 

65 

2 

9 1 

j 

30 

5 1 

r-  107 

63  J 

1 

15  1 

5 ! 

45  ! 

1 

> 92 

27  J 

7 

12 

16 

303 

114 


THE  NORTHERN  BITUMINOUS  COAL  FIELD. 


[BULL.  65. 


Section  under  Murray sville , Pennsylvania. — At  Murraysville,  West- 
moreland County,  Pennsylvania,  in  the  celebrated  natural  gas  region, 
the  top  of  the  Lower  Coal  Measures  lies  60  to  75  feet  below  the  surface, 
and  the  structure  of  the  series  is  thus  given  (Fig.  71) 
by  Mr.  Doubleday,  from  the  records  of  a gas  well  on 
the  Remaley  farm,  Geological  Survey  of  Pennsylvania, 
1SSG,  p.  721 : 


Under  Murraysville , Westmoreland  County,  Pennsylvania. 

[See  map,  I n.] 


Ft. 


( Coal V 

1.  Coal,  Upper  Freeport < Slate 5' 1 

(Coal 4'! 


2.  Slate 

3.  Coal,  slate  in  center. 

4.  Slate 


Fig.  71.— Section 
under  Murrays- 
ville, Pa. 


5. . Sandstone 

6.  Slate 

7.  Slate  and  shells 

8.  Massive  sandstone,  top  of  XII. 


* I 


Ft 

10 


135 


Total. 


236 


Section  on  Beaver  Run , Westmoreland  County , Pennsylvania. — About 
9 miles  northeast  of  Murraysville  a well  was  drilled  on  Beaver  Run, 
beginning  only  4 feet  below  the  level  of  the  Upper  Freeport  coal.  The 
record  (Fig.  72)  of  this  well,  as  given  by  Mr.  J.  A.  Mebaffey,  shows 
the  following  structure  there  (Pennsylvania  Geological  Survey,  1886, 
p.  728) : 


16’ 

20' 

S’ 

6' 

If 

st 

si 

§^rm 

% 

ar 

If 

■SS7: 3=== 

s’J 

Beaver  Bun,  Westmoreland  County,  Pennsylvania. 


8S’ 


Fig.  72. — Section  on 
Beaver  Run,  Pa. 


[See  map,  H n.J 

1.  Coal,  Upper  Freeport 

2.  Concealed 

3.  Black  slate 

4.  Limestone 

5.  Coal,  Lower  Freeport  . 

6.  Fire  clay 

7.  Shell,  hard 

8.  Shale,  soft 

9.  Slate,  black 

10.  Shale,  soft 

11.  Slate,  black 

12.  Coaly  slate,  Upper  Kittanning 

13.  Sandstone 

14.  Slate,  black 

15.  Sandstone,  gray 

16.  Slate,  black 

17.  Sandstone 

18.  Coal,  Lower  Kittanning 

19.  Fireclay 

20.  Iron  ore 

21.  Shales,  soft 

22.  Fireclay 

23.  Pebbly  srndstone,  top  of  XII. 


Ft 


Ft.  in. 
3 6 


5 J 


Total . 


77 


85 

4 

‘25 

6 

2 

18 

276 


WHITE.] 


THE  LOWER  COAL  MEASURES. 


115 


Section  near  Richmond , Pennsylvania. — In  the  northern  portion  of 
Indiana  County,  Pennsylvania,  in  the  vicinity  of  Richmond  village, 
the  Lower  Coal  Measures  exhibit  the  following  struc- 
ture (Fig.  73)  according  to  Mr.  Wm.G-.  Platt,  H4.  p.  266: 

Near  Richmond,  Indiana  County , Pennsylvania. 

Ft. 


12  j 

TV  ■ 

'«*  L 

|^=  ===='5==-.^^ 

==~-===r;-== ' 

20 1 

=•  ==L-=.r= 

J 

I5r 

Ilf 

io'  : 

K' 

s* 

to' 

Z5'  * 

: T 

i- 

45’ 

atfl 

io'  J 

4' 

20 

===■^1=-= 

r 

Er  = =;= 

30* 

5.  Coal,  Lower  Freeport . . . 


[See  map,  F p.] 

1.  Coal,  Upper  Freeport 

2.  Clay - 

3.  Limestone 

4.  Shales  and  thin  sandstone 

Coal...  thin  ) 
Shales.  15'  > .. 
Coal...  thin  ) 

6.  Concealed 

7.  Sandstone 

8.  Clay  slate 

9.  Coal,  Upper  Kittanning.. 

10.  Concealed - 

11.  Shales 

12.  Sandstone 

13.  Slate  and  shales 

14.  Coal,  MiddleKittanning 

15.  Interval 

16.  Coal.  Lower  Kittanning 

17.  Interval 

18.  Shales 

19.  Limestone,  Ferriferous 

20.  Shales  and  slates 

21.  Coal,  Clarion 

22.  Shales 

23.  Sandstone,  massive,  top  of  XII. 

Total 


10 

10 

5 

5 ) 

10  1 
25  f 

5 J 


Ft.  in. 


42 


15 


25 


281  6 


Fig.  73. — Section  near 
Richmond,  Pa. 


Section  near  Lockport  and  Bolivar , Indiana  County , 
Pennsylvania. — In  the  vicinity  of  Bolivar  and  Lockport 
just  east  of  the  Chestnut  Ridge  anticlinal,  Mr.  Wm.  G.  Platt  finds  the 
following  succession  (Fig.  74)  for  these  measures  as  given  in  H4,  p.  65: 

Near  Lockport  and  Bolivar,  Indiana  County,  Pennsylvania. 

[See  map,  I p.] 

1.  Coal,  Upper  Freeport 8 

2.  Clay  shales  6 ] 

3.  Shales,  with  ore  masses 3 

4.  Sandstone  and  sandy  shales 10  [ 

5.  Fire  clay,  good 3 } 52 

6.  Limestone,  impure,  Upper  Freeport 8 

7.  Thin  bedded  sandstone 7 | 

8.  Clay  slates  and  shales 15  j 

9.  Coal,  Lower  Freeport 2 9 

10.  Clay,  impure 3 ] 

11.  Limestone,  Lower  Freeport 5 j 

12.  Clay  shales 10 

13.  Sandstone 7 

14.  Sandy  fire  clay 3 

15.  Slates  and  shales 20 

16.  Sandstone 10 

17.  Grayish  slates %. . . 6 

i i , j mu  ii  . i mi  18.  Coai,  Upper  Kittanning » 1 10 

J ]9.  Fire  clay,  impure 6 ] 

20.  Limestone,  Johnstown  cement 3 I 

.,  . ,i  21.  l)ark  slates  and  shales 20 

t P36  22.  Sandy  shales  with  ore  nodules. 20 

" * ~ 23.  Carbonate  iron  ore  band 0 

24.  Black  slates 10 

25.  Coal,  Middle  Kittanning 

26.  Slates 8 

27.  Shales 10 

28.  Black  slate  and  shale 30 

I 29.  Coal,  Lower  Kittanning 

' 30.  Clay 5 

31.  Sandstone 10 

32.  Shales  and  clay  slates 13 

f Coal  thin  1 

33.  Clarion  coal < Sandstone..  5' > 6 

( Coal 1') 

34.  Fire  clay 2 

35.  Shales 10 

Fig.  74. — Section  near  36.  Sandstono,  heavy,  compact. 

Lockport  and  Boii-  

var,  Pa.  Total 2881 


64 


59 


48 


28 


116 


THE  NORTHERN  BITUMINOUS  COAL  FIElD, 


[bull.  65. 


Section  near  Lauglilinstoicn , Pennsylvania. — In  the  vicinity  of  Laugh- 
linstown,  Westmoreland  County,  and  10  miles  south  from  Bolivar,  Dr. 
Jno.  J.  Stevenson  (KKK,  p.  135)  reports  the  Lower  Coal  Measures  with 
the  following  structure  (Fig.  75) : 

Laurel  Bun,  Ligonier  Township , Westmoreland  County,  Pennsyl- 
vania. 

[See  map,  J p.]  Ft.  in.  Ft.  in. 


Z-- 

zsS 

k' 

Hill 

mu 

mu 

i 

ro' 

a 

S' 

gH i^p 

30' 

*5' 

za' 

» 

33. 

iiiia 

20' 

s' 

g' 

Zh‘ 

Fig.  75.— Section  on 
Laurel  Eun,  Pa. 


1.  Coal,  Upper  Freeport 

2.  Clay 6 

3.  Fire  clay,  non-plastic * 2 

4.  Sandstone 1 

5.  Concealed 11 

6.  Sandstone 1 

7.  Concealed 29 

8.  Shale 12 

9.  Coal,  Lower  Freeport 

10.  Shales 10 

11.  Concealed - 8 

f Coal V 6") 

12.  Coal,  Upper  Kittanning  < Sbaly  sandstone 5'  0"  s 

(Coal 0'  l"i 

13.  Shale 1 

14.  Limestone,  Johnstown  ^ g^™j®stone ^ ^ 

Cement ( Limestone’  II  !*.  1 1!  V.V  0") 

15.  Shale 30 

16.  Coal,  Middle  Kittanning 

17.  Concealed 25 

18.  Sandstone 25 

19.  Shale 1 

f Coal P 10"  1 

| Clay O'  2"  | 

20.  Coal,  Lower  Kittanning  <(  Coal F 0"  )- 

i Coal,  slaty 0'  6"  j 

• [Carbonaceous  shale.. V 8"J 

21.  Clay 

22.  Massive  sandstone,  coarse 

23.  Shale 

24.  Iron  ore 

25.  Shale 

26.  Coal,  Clarion 

27.  Shale 

28.  Ton  of  No.  XIL 


> 

6 $ 


Total 


62 


42  6 

3 6 

51  6 

5 2 


295  9 


Section  on  Cucumber  Bun , Stewart  Township , Fayette  Comity,  Pennsyl- 
vania.— Id  this  same  basin  (Ligonier)  and  on  southwest- 
ward  near  the  Youghiogheny  Biver,  in  Fayette  County, 
the  Lower  Coal  Measures  exhibit  the  following  structure 
(Fig.  76)  on  Cucumber  Bun,  as  reported  by  Stevenson 
(KKK,  p.  89) : 

Cucumber  Bun,  Stewart  Township , Fayette  County,  Pennsylvania. 

Ft.  Ft.  in. 


[See  map,  K n.] 

1.  Coal,  Upper  Freeport 

2.  Clay 

3.  Limestone,  Freeport 

4.  Fire  clay,  Bolivar,  and  shale 

5.  Shale,  sandy 

6.  Coal,  Lower  Freeport  (?) 

7.  Shale,  sandy 

( Coal 2' 

8.  Coal,  Upper  Kittanning(?)  < Clav O'  4 

(Coal 3'  4" 

9.  Clay 


l\ 


44 


10.  Sandstone,  Freeport(?). 
' * itly 


11.  Concealed  (mostly  sandstone)  .. 

12.  Coal,  Middle  Kittanning 

13.  Sandstone 

14.  Concealed 

15.  Coal,  Lower  Kittanning 

16.  Concealed 

17.  Coal,  Clarion  orBrookvillo 

18.  Shah  and  clay 

Fig.  76. — Section  on  19.  Sandstone,  massive,  top  of  XII. 

Cucumber  Eun,  Fay- 
ette County,  Pa.  ‘ Total 


l\ 

0) 


0 8 
30 

5 11 
83 

blossom 

35 

blossom 

60 

2 3 

10 

273  10 


WHITE.] 


THE  LOWER  COAL  MEASURES. 


117 


Section  at  ffewburg,  West  Virginia . — Newburg,  on  the  Baltimore  and 
Ohio  Railroad,  in  Preston  County,  West  Virginia,  is  situated  at  the 
center  of  the  same  coal  basin  as  Bolivar,  Ligouier,  etc.,  and  there  a 
deep  shaft  reveals  the  following  structure  (Fig.  77)  for  the  Lower  Coal 
Measures : 

Shaft  at  Newhurg , Preston  County , West  Virginia. 


[See  map,  O m.] 


Ft.  in. 


1.  Coal,  Upper  Freeport j CoS  and  slate.":  2'  4"  } 

2.  Shales 8 

3.  Sandstone 18 

4.  Limestone,  Upper  Freeport 8 

5.  Shales 6 

6.  Iron  ore 1 

7.  Shales . 4 

8.  Fire  clay  (horizon  of  Lower  Freeport  coal) 

9.  Shales,  gray 14 

10.  Shale,  dark 11 

11.  Shale,  gray 9 

12.  Sandstone,  Freeport 74 

(Coal VO"] 

13.  Coal  Tipper  and  Middle  J % gill. 

Kittanning  ] Fire  ciay*.  2'  0"  | 

[Coal,  good.  2'  0" ) 

14.  Fire  clay  and  shales  with  iron  ore  nodules 


Coal 0'  10"  1 

Shale,  gray O'  10"  I 

Coal  O'  6"  I 

15.  Coal,  Lower  Kittanning  <(  Coal,  bony O'  3"  > .. 

1 Coal,  main  bench. 4'  6" 

I Black  slate 0'  6" 

[Coal 2'  0". 


16.  Sandstone  and  shale 

17.  Pebbly  sandstone,  top  of  XII. 


Ft.  in. 
5 4 


45 


Fig.  77  — Section  at 
Newburg,  W.  Va. 


Total. 


108 

7 3 

15 

9 5 

38 

230 


Here  the  Upper  Freeport  coal  lies  150  feet  below  drainage  and  700 
feet  below  the  tops  of  the  immediate  hills. 

No.  13  appears  to  represent  both  the  Upper  and  Middle  Kittanning 
coal  beds,  which  are  brought  practically  together,  and  also  very  close 
to  the  Lower  Kittanning  bed  by  the  thinning  away  of  intervening 
rocks. 

The  interval  under  the  Lower  Kittanning  bed  here  is  revealed  by  a 
diamond  drill  hole  which  was  put  down  150  feet  below  the  latter 
stratum. 

The  Lower  Freeport  coal  is  not  present,  but  its  horizon  is  clearly 
indicated  by  the  bed  of  fire  clay,  No.  8,  at  45  feet  under  the  Upper 
Freeport  coal. 

The  Freeport  sandstone,  No.  12,  has  a large  development,  and  where 
it  comes  to  the  surface,  4 miles  above  Newburg,  is  nearly  100  feet 

thick. 


118 


THE  NORTHERN  BITUMINOUS  COAL  FIELD. 


fBULL.  65. 


Section  at  Johnstown , Pennsylvania. — Johnstown,  Pennsylvania,  lies 
just  east  of  the  Laurel  Hill  anticline,  and  the  Lower  Coal  Measures 
have  there  been  splendidly  exposed  through  the  mining  operations 
of  the  Cambria  Iron  Company.  The  following  section  (Fig.  78)  of  the 
rocks  in  that  region  is  given  by  the  chief  engineer  of  the  Cambria 
Company,  Mr.  John  Fulton  (H3,  pp.  308,  309) : 


Vicinity  of  Johnstown,  Cambria  County,  Pennsylvania. 


[See  map,  I q.] 


Coal,  Upper  Freeport. 
Fire 


clay. 


Ft. 

1 


Shales 5 

Sandstone 10 

Shales 5 

6.  Kidney  ore '. 0 

7.  Shales 15 

8.  Sandstone i 15 

9.  Shales 3 

10.  Coal,  Lower  Freeport 

11.  Shale 0 

12.  Limestone,  Lower  Freeport 3 

13.  Iron-stained  shales 17 

14.  Sandstone,  gray,  micaceous 21 

15.  Slates 4 

16.  Coal,  Upper  Kittanning 

17.  Fireclay 0 

18.  Limestone,  Johnstown  Cement 5 

19.  Fire  clay,  impure 7 

§ 20.  Slates,  with  iron  ore 8 

21.  Slate 8 

22.  Black  slates,  with  iron  ore — It 

(Coal 0'  3") 

23.  Coal,  Middle  Kittanning  < Slate 1'  0"  > 

(Coal 0'  3") 

24%  Thin  black  slates 13 

25.  Coal r 0 

26.  Fire  clay 4 

27.  Sandstone,  gray 13 

28.  Sandstone,  wavy,  gray 4 

29.  Iron-stained  slates  6 

30.  Coal,  Lower  Kit  tanning 

31.  Fire  clay.. 3 

32.  Gray  slates  and  shales 21 

33.  Massive  black  shales : 15 

34.  Gray  sandstone 5 

35.  Massive  black  slate 5 

36.  Coal,  thin 

37.  Black  slates i 

38.  Gray  sandstone 4 

39.  Thin  gray  slates 6 


54.1&" 


45V 


4hV 


( Coal.. 

40.  Coal,  Clarion Slate  . 

( Coal.. 


4'  6") 
0'  6" } 

1'  10"  ) 


EHE  26 


41.  Fireclay 

42.  Gray  slates 

43.  White  massive  sandstoue,  top  of  XII. 


10 


Ft.  in. 
3 0 


54  10 


2 6 


45  6 


39  9 


1 6 


40  9, 


3 6 


V 60  0 


6 10 


Fig.  78.— Section  near 
Johnstown,  Pa. 


Total. 


3 0 

28  0 


292  8 


WHITE.] 


THE  LOWER  COAL  MEASURES. 


119 


Section  at  Gonemaugh , near  Johnstown , Pennsylvania , — The  writer 
compiled  a section  of  the  Lower  Coal  Measures  atConemaugh  and  else- 
where in  the  vicinity  of  Johnstown,  which  differs  only 
in  minor  details  from  that  of  Mr.  Fulton.  It  reads  as 
follows  (Fig.  79) : 


nm 


3r6f 


46' 


40' 


Is- 


Fig.  79. — Section  at 
Conemaugh,  Pa. 


1.  Coal,  Upper  Freeport 

2.  Fire  clay  »nd  sandy  .shales 

3.  Coal,  Lower  Freeport 

4.  Shales  and  sandy  beds 

5.  Sandstone,  massive  

6.  Coal,  Upper  Kittanning  . . . 

7.  Shale 


Near  Johnstown , Pennsylvania. 

[See  map,  I q.] 


8.  Limestone,  Johnstown 


Limestone 2'  6" 

Shale  and  iron  ore.l'  6" 


9. 


Cement (Limestone 4' 

Dark  sandy  shales  with  iron  ore 33 

Coal  and  slate.. O'  6" 

Slate 0'  6" 

Slaty  coal O'  10'' 


Ft.  in. 


10.  Coal,  Middle  Kittanning. 


11.  Shales,  drab 

12.  Coal 

13.  Impure  fire  clay 

14.  Sandstone,  gray  micaceo 

15.  Sandy  shales 

16.  Coal,  Lower  Kittanuing 

17.  Shales,  sandy 

18.  Coal,  Clariqn 

19.  Fire  clay 

20.  Concealed  and  shales... 

21.  Top  of  xn. 


Ft.  in. 
3 6 

40 

0 7 

20 
40 

3 


> 44 


1 10 


. 15 
. 1 

1 

5 

[ ,71 

. 45 

1 

. 5 

J 

3 

30 

5 

5 

15 

Total . 


281  11 


Section  in  Jackson  Township , Cambria  County , Pennsylvania. — In  Jack- 
son  Township,  Cambria  County,  8 miles  northeast  of  Johnstown,  a 
well  was  once  drilled  for  oil,  and  I obtained  from  the  con- 
tractor the  following  record  (Fig.  80)  of  the  strata  repre- 
senting the  Lower  Coal  Measures.  It  is  chiefly  important 
as  giving  the  total  thickness  of  the  series  in  a vertical 
measurement: 

Jackson  Township,  Cambria  County , Pennsylvania. 

[See  map,  I q.J 


Ft.  in. 


1.  Coal,  Upper  Freeport 3 

2.  Fire  clay  and  slate 6 

3.  Sandstone,  gray 44 

4.  Slate,  drab 2 

5.  Coal,  Lower  Freeport 4 

6.  Fire  clay  and  limestone 6 

7.  “Soapstone”  (shale) 56 

8.  Sandstone,  gray 36 

9.  Coal  and  slate,  Lower  Kittanning 6 

]0.  Sandstone,  gray 48 

11.  Shale 3 

12.  Coal,  Clarion 6 

13.  Fire  clay 3 

14.  Slate,  gray 55 

Fig.  80. — Section  15.  Hard  sandstone,  top  of  XII. 

in  Jackson  Town-  

ship,  Cambria 
County,  Pa. 


55’ 


Total 279 


120 


THE  NORTHERN  BITUMINOUS  COAL  FIELD. 


[hull.  65. 


Section  on  Berts  Greek , Cambria  County , Pennsylvania. — ]^ear  tbe 
eastern  border  of  Cambria  County,  along  the  waters  of  Ben’s  Creek,  in 
Washington  Township,  the  following  section  (Fig.  81)  is  reported  by 
Mr.  Franklin  Platt  (H2,  p.  48) : 

Berts  Creek,  Cambria  County,  Pennsylvania. 


[See  map,  I q.] 


1.  Coal,  Upper  Freeport 

2.  Fire  clay 

3.  Black  slates  and  shales 

4.  Limestone,  Upper  Freeport 

5.  Interval 

6.  Sandstone 


7.  Coal,  Lower  Freeport. 


(Coal O'  2"1 

J Sandstone 2'  0"  ( 

) Fire  clay  and  shale...  6'  0" 

(Coal 2'  0"J 


8.  Fire  clay 

9.  Limestone,  Lower  Freeport 

10.  Shales,  iron-bearing 

11.  Coal,  smnt 

12.  Fire  clay,  shales,  with  ore  balls. 

13.  Coal,  smut 

14.  Fire  clay 

15.  Slates  anil  shales 

16.  Black  slates 

17.  Coal,  Upper  Kittanning 

18.  Fire  clay 


Fig.  81.— Section  on  Ben’s 
Creek,  Cambria  County, 

Pa. 


19.  Drab  shales 

20.  Sandstone,  fine  grained 

2L  Black  slate 

22.  Coal,  slaty,  Middle  Kittanning. 

23.  Fire  clay 

24.  Sandstone 

25.  Fire  clay,  shale 

26.  Black  slate 

27.  Coal,  Lower  Kittanning 

28.  Sandstone  and  shale 

29.  Coal.  Clarion 

30.  Fire  clay 

31.  Sandstone 

32.  Dove-colored  shale,  with  ore  — 

33.  Sandstone 

34.  Fire  clay,  shale 

35.  Coal,  Brookville 

36.  Fire  clay 

37.  Concealed 

38.  Top  of  XII. 

Total 


Ft.  in.  Ft.  in. 

4 4 


6 

15 


15 

12 


\ 55 

J 


10  2 


2 1 

2 6 


15 

0 2 

i 

5 ^ 

0 3 

1 # 


38  11 


7 


56 


9 


2 


5 1 

10  J.  20 

5 J 

3 

18 

5 

5 1 

0 10  | 

10  j>  20  10 


1 8 


25 


263 


2 


WHITE.] 


THE  LOWER  COAL  MEASURES. 


121 


Section  near  Stoyestmcn , Pennsylvania. — In  the  vicinity  of  Stoyes- 
town,  on  Stony  Creek,  Somerset  County,  Pennsylvania,  near  the  center 


11“' 


fi5 


Fig. 82. — Section  near 
Stoyestown,  Pa. 


of  the  basin  between  the  Viaduct  and  Negro  Mountain 
anticlines,  the  series  exhibits  the  following  structure 
(Fig.  82)  according  to  Mr.  Franklin  Platt  (H3,  p.  129) : 

Stoyestoivn,  Somerset  County , Pennsylvania. 


[See  map,  J q.] 


1.  Coal,  Upper  Freeport .. 


2.  Interval 

3.  Black  slates 

4.  Coal,  Lower  Freeport 

5.  Fireclay 

6.  Limestone,  Lower  Freeport 

7.  Interval 

8.  Sandstone,  massive 

9.  Black  slates 

10.  Coal,  Upper  Kittanning 

11.  Black  .slate 

12.  Limestone,  Johnstown  Cement 

13.  Fireclay 

14.  Interval 

15.  Black  slates 

16.  Coal,  Clarion 

17.  Interval,  concealed 

18.  Top  of  No.  XII. 

Total 


Coal 3' > 

Shale 8'  > 

Coal ...  3'  ) 


Ft.  in.  Ft.  in. 


14 


3 

2 

7 

30 

8 

0 

7 

? 

85 

3 


70 

0 


G 


272  6 


Section  at  Pinkerton  Point , Pennsylvania. — On  the  Castleman  River 
at  Pinkerton  Point,  in  the  southern  portion  of  Somerset  County,  a very 
complete  section  of  the  Lower  Coal  Measures  was  obtained  by  Mr. 
Franklin  Platt  along  the  Baltimore  and  Ohio  Bailroad,  near  Shoo  Fly 
Tunnel,  and  is  reported  as  follows  (Fig.  83)  (EL3,  pp.  202, 203) : 


H 


Pinlcei'ton  Point,  Somerset  County,  Pennsylvania. 


[See  map,  L o.] 


Fig.  83.— Section  at 
Pinkerton  Point, 
Somerset  County, 
Pa. 


Upper  Freeport  Coal  (absent)  ■ 


f Coal 2'  3 

< Shale  and  fire  clay  2'  0 


Coal,  Upper  Kittannin  ^ 

( Coal 1 

Limestone,  Johnstown  Cement 


Black  slate 

Coal,  Middle  Kittanning 


3"  ) 


Coal. 


Coal,  Lower  kittanning 
Fire  clay 


Coal,  Clarion 

Fire  clay 

Sandstone 

Slates,  dark  colored 

Massive  sandstone,  top  of  No.  XII. 

Total 


Ft. 

in. 

Ft. 

2 

65 

77 

10 

s 

5 

6 

) 

1.9 

8 

{ 

j 

90 

7 

j 

1 

3 

6] 

4 

6 

10 

0 

6 

31 

10 

J 

2 

1 

20 

1 

31 

10 

1 

6 

4 

18 

267 

122 


THE  NORTHERN  BITUMINOUS  COAL  FIELD, 


[bull.  65. 


Section  near  Gresson , Pennsylvania . — An  oil  boring  near  Cresson,  on 
the  summit  of  the  Alleghany  Mountains,  gives  the  following  measure- 
ments (Fig.  84)  for  the  Lower  Coal  Measures  (H2  page 
30): 

Boring  at  Cresson , Cambria  County , Pennsylvania. 

[See  map,H  r.] 


Ft.  in. 

1.  Coal,  Upper  Freeport 5 

2.  Limestone,  Upper  Freeport 2 

3.  Mixed  drilling 39 

4.  Coal,  Lower  Freeport 4 

5.  Shelly  “soapstone”  (sandstones  and  shales) 115 

6.  Cannel  coal * 0 10 

7.  Slate 35 

8.  Coal,  mixed  with  sandstone w 49 

9.  Hard  sandstone  (No.  XII). 

Total 249  10 

Section  at  Bennington , Pennsylvania. — Just  over  the 
crest  of  the  Alleghany  Mountains,  at  Bennington,  Blair 
^ea^c'resson^a11  County,  the  following  section  (Fig.  85)  of  this  series  has 
been  carefully  worked  out  by  Mr.  John  Fulton  and 
Franklin  Platt  (H2,  pp.  3,  4) : 


hT 


isT 


Bennington , Blair  County , Pennsylvania. 

[See  map,  Hr.] 

Ft.  in. 

Coal,  Upper  Freeport 

Fire  clay,  impure 2 ) 

Sandstones  and  black  slates 20  I 

Limestone,  Upper  Freeport 3 ^ 

Ferruginous  slates  ami  shales 20 

Sandstones  and  sandy  shales. 20  j 

7.  Coal 

Fire  clay 1 1 

Sandstone,  drab 21  } 

10.  Black  slates 20 

11. 

12. 

13 

14, 

15, 

16,  Slates  12  6 j 


Coal,  Upper  Kittanning. 

Drab  slates,  with  iron  balls 11 

Sandstone 0 

Blue  slates 13 

Sandstone,  massive 15 


'.  Coal, 


( Coal 

...O' 

6"  ) 

Middle  Kittann>ng. . . 

. < Slate  — 

...  0' 

6"  > 

( Coal 

...  V 

Fire  clay,  impure 6 

Sands  one 12 

Slate 1 

Coal 0 

Sandstone 7 

Black  slates  8 

Coal,  Lower  Kittanning 


Shales .• 

Black  slates 

Coal,  Clarion 

Slates  

Gray  sandstone ... 

Coal,  Brookville. 

Fire  clay 

Sandstone,  massive,  No.  XII. 

Total 


Ft.  in. 
5 6 


65 

3 

42 

2 10 
52  1 

2 8 


35 


3 

29 

V 34 

2 

1 

23 

4 

} 27 

4 

5 

Fig.  85.— Section  at 
Bennington,  Pa. 


283  8 


WHITE.] 


THE  LOWER  COAL  MEASURES. 


123 


Section  at  Clearfield , Pennsylvania . — At  the  town  of  Clearfield,  Clear- 
field County,  Pennsylvania,  the  following  section  (Fig.  86)  was  made 


by  the  writer : 


Clearfield,  Pennsylvania . 

[See  map,  E s.] 

( Coal,  bony.  V 3"] 

I.  Coal,  Upper  Freeport  ...<j  gjjj;  f_°°^  J',  y>  > 

I Coal.  "I"”  r 6"  j 

2.  Concealed,  and  shales 

3.  Coal,  Lower  Freeport 

4.  Shales 

5.  Sandstone,  massive,  gray,  Freeport 

6.  Shales,  sandy *1 

7.  Coal,  Middle  Kittanning 

8.  Shales,  and  concealed 

9.  Coal,  Lower  Kittanning  

10.  Sandy  shales 

II.  Fir  e clay 

1 2.  Sandstone,  flaggy - 

13.  Shales, dark  

( Coal,  slaty V 6"  I 

14.  Coal,  Clarion < Fire  clay'and  shales.  8'  0"  > 

( Coal,  good 1-  0"  ) 

15.  Fire  clay  and  shales 

( Coal,  slaty.  O'  4") 

16.  Coal,  Brookville — < Shale O'  12"  > 

(Coal O'  8"  ) 

17.  Fire  clay  and  concealed 

18.  Hard  massive  sandstone,  top  of  No.  XII,  in  bed  of  Sus- 

quehanna Elver. 

Total i.. 


Ft.  Ft.  in. 

4 4 


50 

•2 

6 

10 

35 

[ 

70 

25 

s 

1 

6 

35 

2 

25 

j 

8 

6 

V 

f 

45 

6 

J 

10 

6 

10 

* 2 

5 


237  10 


Section  near  Morrisdale , Pennsylvania. — "Near  Morrisdale,  Clearfield 
County,  the  following  section  (Fig.  87)  is  reported  by  Mr.  H.  Marty n 
Chance  (H7,  p.  61) : 

Near  Morrisdale,  Clearfield  County,  Pennsylvania. 


Fig.  87.— Section  near 
Morrisdale,  Pa. 


[See  map,  Ft.] 

1.  Coal,  Upper  Freeport - 

2.  Fire  clay  and  shales 

3.  Coal,  Lower  Freeport 

4.  Fire  clay 

5.  Limestone,  Lower  Freeport - 

C.  Slate  and  sandstone 

7.  Coal,  Upper  Kittanning 

8.  Fire  clay 

9.  Limestone,  Johnstown  Cement 

10.  Fire  clay  and  sandstone  with  iron  ore 

11.  Black  slate 

12.  Coal 

13.  Sandstone 

C Coal 0'  6"  i 

14.  Coal,  Middle  Kittanning.  < Sandstone.  3'  3 " > 

(Coal 0'  10"  ) 

15.  Sandstone 

16.  Slate 

17.  Coal,  Lower  Kittanning 

18.  Interval  to  top  of  No.  XII,  estimated,  about 

Total 


Ft.  in. 


8 10 
8 9 

0 9 

15  6 


25  8 i 

3 4 l 


Ft.  in. 
2 6 
32  6 

4 6 

43  6 

2 10 


39  6 


4 7 
29 

5 6 
75 

239  5 


124 


THE  NORTHERN  BITUMINOUS  COAL  FIELD. 


[BULL.  65. 


Section  at  Sterling  Mines,  near  Houtzdale,  Pennsylvania. — At  the 
Sterling  mines  of  R.  H.  Powell’s  Sons  & Co.,  Clearfield  County,  a 
diamond-drill  boring  was  sunk  through  the  Lower  Coal  Measures,  be- 
ginning 10  feet  below  the  level  of  the  main  coal  mined  in  that  region. 
I copied  the  record  of  this  bore  hole  from  the  office  of  the  company, 
and  it,  combined  with  the  surface  exposures,  gives  the  following  suc- 
cession (Fig.  88) : 


Boring  at  Sterling  Mines , near  Houtzdale,  Clearfield  County,  Pennsylvania . 


1.  Coal,  Upper  Freeport.. . 

2.  Concealed 

3.  Surface  material  in  drill 

4.  Dark  slate 


[See  map,  G s.] 

f Done  coal 0'  10"  ? 

I Coal,  sometimes  a thin  slate  in  center..  4'  6"  5 


liole. 


5.  Coal,  Lower  Freeport. .. 

6. 

2‘  7. 


f Black  shale  and  coal 1'  6"  1 

I Shale,  sandstone,  and  slate 8'  6" 

Soft  shale 1'  0"  } 

I Sandstone V 0"  j 

( Coal  1'  0"  J 


50' 


Fig.  88. — Section  at 
Sterling  Mines, 
near  Houtzdale,  Pa. 


Sandy  shale 

Hard  sandstone,  Freeport 

Dark  slate 

Coal,  Upper  Kittanning . . . 

Fire  clay 

Dark  slate 

Coal,  Middle  Kittanning  . . 
Slate 


Sandy  shale 

Slate 

Coal,  Lower  Kittanning 

Fire  clay 

Slate 


Sandstone,  close,  hard . 

Shales 

Coal,  Clarion 

Hard  slate 


Ft 


10  1 

16  \ 
16  J 


7 J 

n 

9 

32 

21 


Ft.  in. 
5 4 


42 


13 


50 


33 


Total. 


63 


241  4 


The  coal  at  the  top  of  this  hist  section  has  been  identified  as  the 
Lower  Freeport  bed,  throughout  the  Clearfield  region,  by  Messrs.  Platt, 
Chance,  and  other  Pennsylvania  geologists  ; but  it  seems  to  me  that 
this  section,  taken  in  connection  with  the  one  at  Clearfield  (Fig.  86), 
tends  to  prove  that  the  coal  in  question  is  the  Upper  Freeport.  This 
interpretation  is  further  confirmed  by  the  presence  of  the  Lower  Ma- 
honing sandstone  on  above  No.  1,  and  a thin  coal,  the  Mahoning  bed, 
at  60  to  80  feet  above  the  latter,  while  crowning  the  hills  is  the  Upper 
Mahoning  sandstone,  whose  top  is  100  feet  above  No.  1.  Then,  too,  the 
structure  of  the  coal  itself  is  the  same  as  the  Upper  Freeport,  a few 
miles  distant,  where  it  is  mined  along  the  Pennsylvania  Railroad,  in 
the  edge  of  Blair  County.  , 


WHITE.  1 


THE  LOWER  COAL  MEASURES. 


125 


Section  at  Shoup’s  Run , Broad  Top  Basin , Huntingdon  County , Penn- 
sylvania.— In  the  Broad  Top  coal  basin,  Shoup’s  Bun,  Huntingdon 
County,  Pennsylvania,  the  Lower  Coal  Measures  exhibit 
the  following  structure  (Fig.  89),  as  given  by  the  writer 
in  T3,  Geological  Survey  of  Pennsylvania,  page  46  : 


100’ 


so 


Shoup’s  Bun,  Broad  Top  Basin,  Huntingdon  County , Pennsylvania. 


[See  map,  J t.] 


1.  Coal,  Upper  Freeport 

2.  Sandy  shales  and  sandstone . 

3.  Coal,  Upper  Kittanning 

4.  Shales  and  sandstone 

5.  Coal,  Middle  Kittanning 

6.  Shales  and  shaly  sandstone. . 

7.  Coal,  Lower  Kittanning 


Fig.  89. — Section  8-  Shales  and  concealed. .. 

at  Shoup’s  Run,  Massive  conglomerate. 
Broad  lop  Ba- 
sin, Huntingdon 

County,  Pa.  Total 


Ft. 

1 

100 

2 

16 

4 

50 

6 

20 


199 


Section  in  East  Broad  Top  Basin , Huntingdon  County , Pennsylvania. — 
In  the  East  Broad  Top  region  of  Huntingdon  County  the  structure  is 
thus  (Fig.  90)  given  by  Mr.  H.  N.  Sims  (T3,  p.  68) : 

East  Broad  Top  Basin,  Huntingdon  County , Pennsylvania. 


[See  map,  J t.] 


1.  Coal  and  slate,  Upper  Freeport 

2.  Concealed 

•3.  Conglomerate,  small  pehhles 

4.  Massive,  light  gray,  pebbly  sandstone,  slightly  argilla- 

ceous at  top 

5.  Concealed 

6.  Sandstone,  micaceous 

7.  Concealed  to  top  of  shaft 

8.  Dark  gray  slate  with  iron  ore  balls 

9.  Sandstone,  micaceous,  dark  gray 

C Coal 2'  7" 

10.  Coal,  Upper  Kittanning  < Black  slate 

( Coal 

11.  Sandstone,  slaty 

12.  Coal,  MiddlO  Kittanning 

13.  Concealed 

14.  Blue  clay  shales 

15.  Concealed : 

16.  Yellow  shaly  sandstone 

17.  Dark  gray  sandy  slate 

18.  Black  slate,  sandy 


Ft.  in. 
2 


Ft.  in. 

10 

10 


69 

4 6 > 165  4 

2 i 

34  10  ! 


2'  7") 

O' 

O'  2"S 


Fig.  90. — Section  in  Fast 
Broad  Top  Basin,  Hunt- 
ingdon County,  Pa. 


C Coal,  top  bench 1'  6" 

19.  Coal,  Lower  Kittanning  < II  ml  slate,  parting.  0'  4" 
( Coal,  bottom  bench.  2'  0" 


Total 


3 3 
2 9 


35 


3 10 
216  2 


126 


THE  NORTHERN  BITUMINOUS  COAL  FIELD. 


(BULL.  65. 


Section  in  Broad  Top  Basin . Bedford  County , Pennsylvania.— In  tlie 
Broad  Top  Basin  of  Bedford  County,  Pennsylvania,  the  structure  is 
thus  (Fig.  91)  given  by  Stevenson  (T3,  pp.  59  and  60): 


Broad  Top  Basin,  Bedford  County,  Pennsylvania. 


[See  map,  J t.] 

1.  Coal,  Upper  Freeport 

2.  Shales  and  sandstones 

3.  Coal,  Upper  Kittanning 

4.  Clay 

5.  Sandstone 

6.  Coal,  Middle  Kittanning 

7.  Clay 

8.  Sandstone  and  shale 

9.  Coal,  Lower  Kittanning 

10.  Clay 

11.  No.  XII,  conglomerate. 

Total 


Ft. 


50 


Ft.  in. 
5 
93 

1 6 
2 
28 
4 

56 


195- 


& lection  act  Piedmont , West  Virginia. — In  the  vicinity  of  Western  port, 
Maryland,  where  the  North  Potomac  cuts  across  the  Cumberland  or 
George’s  Creek  coal  basin,  the  Lower  Coal  Measures  exhibit  the  follow- 
ing succession  (Fig.  92) : 


Piedmont , Mineral  County , West  Virginia. 


!'  V 


(lllllllllllllllIHll 


Y 

zd 


1.  Coal,  Upper  Freeport. 


Fig.  92. — Section  at 
Piedmont,  W.  Va. 


[See  map,  N p.] 

Coal 2' 

Shale  and  hone.  1 
Coal 2 

Concealed 

Shale,  bluish 

Coal,  Lower  Freeport 

Fire  clay 

Concealed 

Sandstone,  hard 

Sandstone,  shaly 

Shales,  sandstone,  and  concealed 


:i 


Coal,  Upper  Kittanning..  J £j^mill0US  slate 


2'} 


Ft. 


10  ] 

10  3 

2 1 
10  | 
2 
5 

55 


10  1 
50  [> 

5 J 


Dark  shales,  and  concealed 

Massive  sandstone,  gray 

Shales,  drab 

f Coal,  slaty . . 1'  0"  ] 

Coal,  bon  v . o'  8"  ‘ 

Coal,  Lower  Kitlanning  <{  Coal,  good . . 1'  4"  J- 

| Slate,  hard  . ()'  h"  | 

[Coal, good..  2 6 "J 

Fire  clay,  sandy 

Shales,  with  nodular  iron  ore 

Fire  clay,  impure 

Flaggy  sandstone , 

Concealed 

Fire  clay,  sandy 

Flaggy  sandstone  and  sandy  shales 25  J 

Concealed,  and  sandy  shales a 

Top  of  No.  XII. 


3 1 

2 

4 

20  > 
25 
10 


Ft.  in. 
5 


65 


6.J 


8Q 


40 


307  6i 


Total 


WHITE.] 


THE  LOWER  COAL  MEASURES. 


127 


Section  near  Maple  Swamp  water  tank,  West  Virginia  Central  Rail- 
road, Mineral  County,  West  Virginia . — Near  Maple  Swamp  water  tank, 
on  the  West  Virginia  Central  Railroad,  Mineral  County, 
West  Virginia,  these  beds  exhibit  the  following  structure 
(Fig.  93) : 

On  North  Potomac  at  Maple  Swamp  water  tank,  West  Virginia  Central 

Railroad. 


[See  map,  N p.] 


Ft.  in. 

C Coal O'  5") 

1.  Coal,  Upper  Freeport . . < Bone  and  slate . . 1'  4"  > 4 3 

(Coal 2'  6"  } 

2.  Concealed - 60 

3.  Coal,  Lower  Freeport 1 2 

4.  Concealed 55 


Coal,  Upper  Kittanning 
Concealed,  and  slate 


6 


35' 


C Coal 3'  0") 

Coal,  Lower  Kittanning  < Slate 2'  0"  > 

^ (Coal V 5") 

Concealed,  and  sandstone  85 

Coal,  Clarion 2 6 

Shales,  and  concealed 45 

Massive  sandstone,  top  of  No.  XII. 

Total 305  4 


Section  near  Thomas,  West  Virginia. — At  the  head  of 
the  North  Potomac  and  on  the  Cheat  River  side  of  the 
great  Alleghany  watershed,  we  get  a fine  exposure  of  the 
Lower  Coal  Measures  in  the  vicinity  of  Thomas,  Tucker 
County,  West  Virginia.  The  exposures  have  been  made 
by  the  mining  and  grading  operations  of  the  West  Vir- 
ginia Central  Railroad,  and  there  the  section  reads  as  follows  (Fig.  94): 


Fm.93.-On  North 
Potomac  at  Ma- 
ple Swamp  Wa- 
ter Tank,  West 
Virginia  Cen- 
tral .Railroad. 


Near  Thomas,  Tucker  County , West  Virginia. 


[See  map,  O o.] 


1.  Coal,  Upper  Freeport 


Coal 

Bone  and  bony  co; 
Coal 

2.  Sandy  shales,  weathering  reddish 

C Coal 

3.  Coal,  Lower  Freeport . . < Shale 

( Coal 

4.  Concealed  

5.  Massive  pebbly  sandstone,  Freeport 

6.  Coal,  streak,  Upper  Kittanning 

7.  Fire  clay  and  shales 

f Coal,  good 1' 

Slate O' 


8.  Coal,  Middle  and  Lower 
Kittanning 


Fig.  94.  — N ear 
Thomas,  Tucker 
County,  W.Va. 


9.  Concealed 

10.  Massive  sandstone 

11.  Shales 

12.  Iron  ore,  bnhrstone 

13.  Limestone,  ferriferous 

14.  Shales  and  sandstone 

15.  Coal,  Clarion 

16.  Shales  

IT  Sandstone,  top  of  No.  XII. 


Coal,  good 1' 

S.ate 0' 

Coal,  good 3' 

Shale,  gray 1' 

Coal,  slaty 3' 


Ft. 


Ft.  in. 
8 
40 

1 6 
70 
35 


Total 


273  6 


128 


THE  NORTHERN  BITUMINOUS  COAL  FIELD. 


[BULL.  65. 


Section  near  Moatsville,  Barbour  County , West  Virginia. — I^ear  Moats- 
ville, Barbour  County,  West  Virginia,  on  the  Tygart’s  Valley  River, 
the  following  section  of  the  Lower  Coal  Measures  is  ex- 
posed (Fig.  95): 

Near  Moatsville , Barbour  County,  West  Virginia. 


sa' 


Fig.  95. — Section 
near  Moats- 
ville, W.  Va. 


[See  map,  O m.] 

1.  Coal,  Upper  Freeport 

2.  Concealed,  and  sandy  shales  ...  

[ Slatv  coal  and  slate  O'  G" 

| Shale  and  lire  clay..  4'  0" 

3.  Coal, Lower  Freeport..  <1  Coal  ....  2'  0 

Dark  bony  clay O'  3' 

[Coal ' 1'  3" 

4.  Concealed 

5.  Sandstone,  massive,  gray 

6.  Concealed 

7.  Dark  blue  shale 

8.  Flaggy  sandstone  and  concealed 

9.  Limestone,  gray,  Campbell’s  Creek 

10.  Shales,  and  massive  sandstone 

f Coal 

11.  Coal,  Lower  Kittanning < Shales 

( Coal 

12.  Concealed 

13.  White  pebbly  sandstone,  top  of  No.  XII. 


Ft. 


Ft.  in. 
3 

50 


105 


. 1'  6"  ) 
i.  8'  0"  V 
. . 3'  0"  > 


Total 


220  6 


Section  near  Valley  Falls , West  Virginia. — In  the  vicinity  of  Valley 
Falls,  Taylor  County,  West  Virginia,  where  the  Chestnut  Ridge  anti- 
cline brings  the  series  above  water  level,  the  following  succession  is 
visible  (Fig.  96) : 


Valley  Falls , Taylor  County,  West  Virg  nia . 

[See  map,  N 1.] 


3 

AO 

W 

11111 

3 / 

V? 

w 

iaf 

i ) 

¥ 

HUM! 

5' 

& 

zo' 

:m & 

isf 

l c 

a' 

Coal,  Upper  Freeport 
Concealed  and  shales 

Sandstone 

Blue  shales 


«a‘  5.  Coal,  Lower  Freeport. 


Dark  shales 

Sandstone,  Freeport 
Shales,  blue 


f Coal O'  3" 

I Slate,  gray 0'  6" 

I Coal ‘ 1'  3'' 

Shale 2'  11" 

I Coal,  bony  cannel.  0'  6" 

I Shale,  gray 0'  8" 

[Coal....... 1'  3" 


Ft. 

40 

15 

4 


Ft.  in. 
3 


59 


7 4 


9.  Coal,  Upper  Kittanning 


10. 
11. 
12. 

13. 

14. 

15. 

16. 

17. 

18. 

19. 

20. 

r45  2i. 

22. 

23. 


Coal 
Shale,  gray 
Coal,  bony 


. . . . 3'  1"  ) 
ay.  0'  1" > 
y..  0'  7"  ) 


?) 


24. 

—Section  25- 


Fig. 

near  Valley  Falls, 
W.  Va. 


Shales,  dark  grayish 

Coal,  Middle  Kittanning 

Shales  and  flaggy  sandstone 

Limestone,  siliceous a . 

Sandstone,  flaggy 2 ( 

Shales,  containing  iron  ore  nodules 5 

Limestone,  dark  blue,  Campbell’s  Creek 1 

Shales 20 

Coal,  Lower  Kittanning 

Fire  clay 5 

Sandstone,  flaggy o 

Sandy  shales,  and  concealed 20 

Sandstone,  hard,  micaceous  15 

C Coal..  O'  2" 

Coal,  Clarion < Shale.  0'  10 

(Coal..  0'  2" 

Shales,  and  concealed 

Sandstone,  massive,  top  of  No.  XII. 


2") 


55 


Total 


258  3 


In  this  last  sectiou,  and  also  in  the  preceding  one  (Fig.  95),  a bed  of 
impure,  siliceous  limestone  occurs  in  the  shale  interval  above  the  Lower 


WHITE.] 


THE  LOWER  COAL  MEASURES. 


129 


Kittanning  coal.  It  occup:es  the  same  geological  horizon  as  the  thin, 
siliceous  limestone  above,  the  Campbell’s  Creek  (Lower  Kittanning) 
coal  on  the  Big  Kanawha  River,  and  hence  I have  identified  it  with 
that  stratum. 


Section  near  Nuzum’s  Mill , Marion  County , West  Virginia. — Farther 
down  the  stream  (Tygart’s  Valley  River)  the  following  structure  (Fig. 
97)  was  observed  on  the  right  bank,  below  Nuzum’s  Mill,  Marion 
County,  West  Virginia: 


Fig.  97.— Section  near 
Nuzum’s  Mill,  Marion 
County,  W.  Va. 


1. 

2. 

3. 


7. 


10. 


13. 


17. 


21. 


23. 


25. 

26. 

27. 

28. 


Near  Nuzum’s  Mill , Marion  County,  West  Virginia. 


[See  map,  N 1.] 

Coal,  Upper  Freeport 

Clay  

Sandstone 

Limestone,  Upper  Freeport 

Shales  and  concealed 

Sandstone,  coarse 

Shales,  sandy,  drab  

Coal,  Lower  Freeport 

Shales  and  concealed  

Massive  sandstone,  Freeport 

Coal,  Upper  Kittanning 

Shales,  dark,  sandy,  with  limy  beds 

Black  slate — 

Coal,  slaty,  Middle  Kittanning 

Shales  and  sandy  beds 

Coal.  Lower  Kittanning 

Fire  clay 

Sandstone,  flaggy 

Dark  shales  with  iron  ore  nodules 

Iron  ore,  Ferriferous  limestone  horizon 

Dark  shales 

Black  slate 

Coal,  Clarion 

Fire  clay,  sandy 

Dark  shales,  with  iron  ore  nuggets  near  middle 

Flaggy  sandstone 

Concealed  and  coal  blossom,  Brookville 

No.  XII,  conglomerate. 

Total - 


Ft.  in. 


2 

15 

3 

13 

10 

15 

30 

25 


1 

I 


t 


J 


40 

3 


5 

5 

12 

0 

5 

2 


1 

1 

i 


Ft.  in. 

3 


58 

5 7 

55 

2 

43 

1 

20 

5 

30 

0 1 

33 

6 


..  261  8 


Fig.  98.— Sect i on 
under  Clarksburg, 
W.  Va. 


Section  under  Clarksburg,  West  Virginia. — From  the 
records  of  the  Despard  gas  well  boring,  at  Clarksburg, 
Harrison  County,  West  Virginia,  as  furnished  by  T.  M. 
Jackson,  civil  engineer,  we  get  the  structure  of  the 
Lower  Coal  Measures  there,  as  follows  (Fig.  98): 

Under  Clarksburg,  West  Virginia. 


[See  map,  O k.] 

1.  Upper  Freeport  coal 

2.  Shales#  sandy  

3.  Sandstone,  white 

4.  Shales 

5.  Sandstone,  white,  Freeport 

6.  Sandstone,  dark  . 

7.  Coal,  Middle  Kittanning 

8.  Shale,  black  

9.  Sandstone,  gray 

10.  Sandstone,  white  

11.  Coal,  with  slate.  Lower  Kittanning 

12.  Sandstone,  hard,  gray  

13.  Sandstone,  bard,  white 

14.  Shale 

15.  Top  of  No.  XII,  white  sandstone. 

Total 


Ft. 

Ft. 

absent 

291 

7 

79 

124 

il  | 

io  i 

Si 

1 

49 

16  ^ 

4 

4) 

36  t 
14  5 

54 

232 


The  Lower  Kittanning  bed  is  here  more  than  1,000  feet  betew  the 
summits  of  the  hills. 

Bull.  65 9 


130 


THE  NORTHERN  BITUMINOUS  COAL  FIELD. 


[BULL.  65. 


Section  under  Parkersburg , West  Virginia. — At  Parkersburg,  Wood 
County,  West  Virginia,  the  following  structure  (Fig.  99)  is  given  by  the 
record  of  the  Camden  Consolidated  Oil  Company’s  drill 
hole,  on  the  authority  of  K.  A.  Cole,  superintendent: 

Under  Parkersburg,  West  Virginia » 

[See  map,  N f.]  Ft. 

1.  Upper  Freeport  coal - absent 

2.  Shales,  gray  and  black 170 

3.  Coal,  Lower  Kittanning 7 

4.  Shales,  gray - 98 

5.  Top  of  No.  XII. 


Total 


275 


Fig.  99. — Section 
under  Parkers- 
burg, W.Va. 


The  Lower  Kittanning  bed  is  the  only  one  in  the  series 
here,  but  it  has  a good  thickness,  though  lying  1,100  feet 
below  the  bed  of  the  Ohio  Kiver,  and  1,500  feet  under 
the  surface  of  the  hill  summits. 

Section  under  Wheeling , West  Virginia. — 

Under  Wheeling,  West  Virginia,  where  the 
top  of  the  series  is  more  than  400  feet  below 
water  level,  the  record  of  the  Central  Glass 
Company’s  drill  hole  for  gas  gives  the  fol- 
lowing structure  (Fig.  100) : 

Under  Wheeling,  West  Virginia. 

[See  map,  Kj.]  Ft. 

g coal  and  450  feet  under 

7 


1.  Coal,  Upper  Freeport— 556  feet  under  Pittsburg  coal  and  450  feet  under 

Ohio  Kiver  level 

2.  Sandstone  and  shales 96 

3.  Coal,  Upper  Kittanning 5 

4.  Shales  and  sandstone 112 

5.  Top  of  No.  XII. 

Total 220 


rrrrrvv?! 


50 


Section  at  mouth  of  Little  Beaver , on  the 
Pennsylvania- Ohio  State  line.  — At  the  ^nd^Vheeto^ 
mouth  of  Little  Beaver,  on  the  Pennsyl-  W-Va- 
vania-Ohio  State  line,  and  the  northern  point  of  the 
West  Virginia  “Pan-Handle,”  the  structure  is  as  fol- 
lows (Fig.  101): 


1.05’ 


Ohio  and  Pennsylvania  line,  v^outh  of  Little  Beaver. 


60' 


Fig.  101. — Section  at 
mouth  of  Little 
Heaver. 


[See  map,  G j.] 

1.  Coal,  Upper  Freeport 

2.  Sandy  shales 

3.  Coal,  Lower  Freeport 

4.  Sandy  shales 

5.  Sandstone,  massive 

6.  Sandy  shales  ..  

7.  Coal,  Middle  Kittanning 

8.  Fireclay - 

9.  Shales,  containing  nodules  of  iron  ore  ..... 

10.  Coal,  Lower  Kittanning 

11.  Fire  clay 

12.  Sandy  shales  and  shaly  sandstone 

13.  Limestone,  Ferriferous 

14.  Sandy  shales 

15.  Bituminous  shale,  Clarion  coal 

16.  Shales,  sandy 

17.  Massive  sandstone,  top  of  No.  XII. 


Ft. 


Ft.  in. 
50 


16 


Total. 


273  6 


WHITE.] 


THE  LOWER  COAL  MEASURES. 


131 


Section  near  Sprucevale , Cotunxbiana  County , Ohio. — Northward  up 
the  Little  Beaver  the  column  of  rocks  is  very  much  the  same  as  at  the 
OhioBiver,  as  may  be  seen  from  the  following  section  (Fig.  102)  taken 
near  Sprucevale,  Columbiana  County,  Ohio  : 


Fig.  102.— Section 
near  Sprucevale, 
Columbiana 
County,  Ohio. 


Near  Sjprucevale,  Columbiana  County,  Ohio. 


[See  map,  G j.] 

1.  Coal,  Upper  Freeport 

2.  Fireclay 

3.  Limestone,  Upper  Freeport 

4.  Shales,  and  concealed 

5.  Coal,  Lower  Freeport 

6.  Concealed 

7.  Sandstone,  massive,  Freeport 

8.  Coal,  Middle  Kittanning 

9.  Concealed 

10.  Coal,  Lower  Kittanning 

11.  Fire  clay  and  shales 

12.  Limestone,  siliceous,  Upper  Ferriferous 

13.  Shales,  gray 

14.  Shales,  dark 

, _ T . . C Lower  Ferriferous  . . ? 

15.  Limestone } Putnam  Hill \ — 

16.  Coaly  .shales,  Clarion . 

17.  Fire  clay 

18.  Concealed,  to  top  of  No.  Xll 

Total 


Ft.  Ft. 


thin 

25 

2 


5 


1 


5 

5 


291 


Here  we  get  the  beginning  of  an  important  feature  in  Ohio  Lower 
Coal  Measure  stratigraphy,  viz : a duplication  of  the  Ferriferous  lime- 
stone. The  lower  bed,  No.  15,  occupies  the  regular  horizon  of  the 
Pennsylvania  u Ferriferous  ” bed,  but  there  comes  in  above  it  here  a 
stratum,  No.  12,  of  siliceous  limestone,  not  seen  anywhere  in  Pennsyl- 
vania, but  becoming  the  ore-bearing  limestone  of  the  Ohio  series,  and 
known  as  the  “ Gray  ” limestone,  the  ore  on  its  top  being  of  the  same 
character  as  the  Buhrstone  ore  of  Pennsylvania  and  apparently  identi- 
cal with  it. 

Prof.  Orton,  director  of  the  Ohio  Geological  Survey,  thinks  that  on 
entering  Ohio  the  Great  Ferriferous  limestone  of  Pennsylvania  splits 
into  two  portions,  the  upper  part  representing  the  “ Gray  ” limestone 
and  the  lower  or  blue  portion  of  the  Ferriferous  representing  the 
“ Putnam  Hill”  bed  of  Ohio.  This  seems  to  be  the  most  probable  view 
of  the  matter,  though  it  is  barely  possible  that  the  lower  or  Putnam 
Hill  stratum  is  an  entirely  new  deposit,  and  has  no  representative  in 
Pennsylvania,  or  this  may  b«  true  with  reference  to  the  upper  limestone, 
No*  12* 


132 


THE  NORTHERN  BITUMINOUS  COAL  FIELD. 


[BULL.  65. 


Section  between  New  Lisbon  and  Leetonia , Ohio . — In  going  northwest- 
ward from  Sprucevale,  a very  rapid  change  takes  place  in  the  lower 
portion  of  the  column,  since  it  rapidly  contracts,  as  will  be  seen  from 
the  following  section  (Fig.  103),  made  in  the  vicinity  of  the  cement 
works,  between  New  Lisbon  and  Leetonia,  Ohio : 


and  Leetonia,  Ohio. 


Between  New  Lisbon  and  Leetonia,  Ohio. 

[See  map,  G i.]  Ft.  Ft.  in. 

Coal,  Upper  Freeport  (not  seen) 

Concealed 30  ^ 

Sandstone 10  > 50 

Shales,  chocolate 10  ' 

Coal,  Lower  Freeport 0 2 

Fireclay 4 

Limestone,  Lower  Freeport 4 

Concealed,  and  sandstone 50 

Shales 5 

Coal,  Lower  Kittanning..  ^ i'  — 6 6 

Slate 1 1 

Limestone  and  iron  ore,  Upper  Ferriferous 1 ! 

Concealed,  and  shales 35  { 39 

Limestone,  fossiliferoos..  { lgg3a*»» } - 2 1 

Coal,  Clarion 3 

Fire  clay 10  > 

Interval  to  top  of  No.  XII 25  3 ^ 

Total 196  8 


Section  near  Zanesville , Ohio. — In  the  vicinity  of  Zanesville,  Muskin- 
gum County,  Ohio,  the  section  of  the  Lower  Coal  Measures  reads  as 
follows  (Fig.  104),  at  the  type  locality  of  the  Putnam  Hill  limestone 
(Vol.  Y,  Ohio  Geology,  p.  96) : 

Zanesville,  Muskingum  County,  Ohio. 


Fig.  104.  — Section 
n ear  Zan  es  ville, 
Ohio. 


[See  map,  K e.] 

1.  Coal,  Upper  Freeport 

2.  Fire  clay 

3.  Limestone,  Upper  Freeport 

4.  Concealed 

5.  Coal,  Lower  Freeport 

6.  Fire  clay 

7.  Concealed 

8.  Sandstone,  Freeport 

9.  Coal,  Middle  Kittanning 

10.  Fire  clay 

11.  Shales,  with  ore  nodules 

12.  Coal,  Lower  Kittanning 

13.  Fire  clay 

14.  Limestone,  Upper  Ferriferous 

15.  Sandstone .. 

16.  Shales 


17.  Limestone... 


Lower  Ferriferous ? 

Putnam  Hill 3 


18.  Shales,  dark 


19.  Coal 

20.  Fire  clay  and  dark  shales 

21.  Coal,  Clarion.. * 

22.  Fire  clay,  shales,  and  concealed,  to  base  of  Lower  Coal 

Measures 


Ft. 

Ft.  in. 

4 

2 l 

1 ( 

42 

39  ’ 

1 

6 ) 

34  [ 

60 

20  J 

4 

6 \ 
18  3 

24 

4 

4 1 

2 [ 
44 

56 

thin 


15 


Total. 


225  0 


THE  LOWER  COAL  MEASURES. 


133 


Section  near  Shawnee  and  McCuneville , Ohio. — In  the  vicinity  of 
Shawnee  and  McCuneville,  Perry  County,  Ohio,  these  beds  exhibit  the 
following  structure  (Fig.  105) : 

Vicinity  of  Shawnee  and  McCuneville,  Perry  County,  Ohio. 


[See  map,  M d.] 

Ft.  in 

1.  Coal,  Upper  Freeport  (not  seen) 

2.  Fire  clay  and  shales  containing  “ Buchtel  ” ore. 15 

3.  Limestone,  Upper  Freeport 2 ( 

4.  Shales,  and  concealed 25 

5.  Coal,  Lower  Freeport 1 ( 

Clay,  with  iron  ore 10 

7.  Concealed,  and  shales 25 

2'  0" 

coal 

Coal 

8.  Coal,  Middle  Kittanning  ■(  dark  gray 


Fig.  105.— Vicinity 
of  Shawnee  and 
McC  u n e v i 1 1 e, 
Perry  County, 
Ohio. 


16.  Fire  clay 10 

17.  Massive  sandstone,  top  of  No.  XII.  


10  8 


Coal. 

Slate O' 

Coal 3' 

Clay,  with  calcareous  ore 10 

10.  Concealed,  and  shales 20 

11.  Coal,  Lower  Kittanning 

12.  Clay  5 

13.  Ferriferous  ore  and  flint 1 

14.  Sandy  shales 40 

is  ( Lower  Ferriferous ? . 

15.  Limestone $ Putnam  Hill j 1 


Total 176  8 


Section  near  Buchtel , Ohio. — In  the  vicinity  of  Buchtel,  at  the  line  of 
Hocking  and  Athens  Counties,  the  Lower  Coal  Measures  exhibit  this 
structure  (Fig.  106) : 

Hocking  Valley,  near  Buchtel,  Athens  County,  Ohio. 

[See  map,  N c.]  Ft.  Ft.  in. 


Fig.  106.— Hock- 
ing Valley,  near 
Buchtel,  Athens 
County,  Ohio. 


( Coal,  slaty 1'  3"' 

j Shale 0'  3" 

I Coal 1'  3" 

1.  Coal,  Upper  Freeport..  <(  Shale 0'  3" 

I Coal. 1'  3" 

Shale 0'  3" 

[Coal 1'  3", 


2.  Fire  clay  and  shale . . 

3.  Limestone,  Freeport 


4.  Concealed,  and  shales 

C Coal V 6 "'k 

5.  Coal,  Lower  Freeport . . < Slate O'  1"  > 

(Coal V 6"} 

6.  Concealed 

(Bone coal O'  6"1 

Coal 2'  0"l 

7.  Coal,  Middle  Kittanning  < ® ’!!!!*!’!!  v %'( 

( Slate."!!.’!”.’.*.’  0'  1" 

l Coal 1'  6"  J 


8.  Concealed 


9.  Coal,  Lower  Kittanning 
10.  Concealed 


11.  Iron  ore 

12.  Limestone,  Ferriferous  ... 

13.  Interval  to  top  of  No.  XII 


Total , 


5 9 


5) 

5 j>  50 
40  j 

3 1 

30 


6 1 


30 

1 

10 

1 

2 

40 


178  11 


134 


THE  NORTHERN  BITUMINOUS  COAL  FIELD. 


[bull.  65. 


Section  on  Meeker's  Run , near  N’elsonville , Ohio. — On  Meeker’s  Run, 
near  Nelsonville,  Athens  Couuty,  Ohio,  the  structure  of  the  Lower 
Coal  Measures  is  thus  (Fig.  107)  given  by  Prof.  Orton  in  Yol.  Ill,  Ohio 
Geology,  page  926 : 

On  Meelcer's  Bun , near  Nelsonville,  Athens  County,  Ohio. 


[See  map,  N c.] 


1.  Coal,  Tipper  Freeport. 

2.  Fire  clay 

3.  Shales  

4.  Buchtelore 

5.  Shales 

6.  Straitsville  ore 


Fig  107.— Section 
on  Meeker’s  Run, 
Athens  County, 
Ohio. 


7.  Shawnee  or  Buff  limestone  (Upper  Freeport) 

8.  Sandstone 

9.  Coal,  Lower  Freeport 

10.  Shales. 

11.  Limestone,  Lower  Freeport . . { } 

12.  Sandstone 

13.  Coal,  Upper  Kittanning  .. 

14.  Fire  clay 

15.  Sandstone 

16.  Shale 

17.  Coal 

18.  Fire  clay 

19.  Shale 

20.  Snowfork  ore 

21.  Sandstone 

22.  Coal,  Lower  Kittanning.. 

23.  Fire  clay 

24.  Shales 

25.  Place  for  Baird  ore 

26.  Place  for  Gray  limestone 

27.  Interval  to  No.  XII  sandstone 

Total 


Middle  Kittanning. 
N elsonville  seam . . . 


Ft.  in. 

4 

3 

5 9 

1 3 

6 
1 

2 6 

14  6 
1 0 

4 0 

1 6 

12  6 
3 

1 6 

15  6 

3 6 

6 11 

3 

5 

0 8 
27 
2 

4 

6 


30 

165  1 


Section  at  Panther  Hill,  Scioto  County , Ohio. — Farther  to  the  southwest, 
in  Panther  Hill,  near  Mt.  Yernon  Furnace,  Scioto  County,  Ohio,  these 
rocks  are  given  as  follows  (Fig.  108)  in  Yol.  Y,  Ohio  Geology,  p.  1038: 


Panther  Hill,  Mt.  Vernon  Furnace,  Scioto  County , Ohio. 


[See  map,  Q a.] 

1.  Coal,  blossom,  Upper  Freeport 

2.  Shale,  sandy 

3.  Concealed - 

4.  Sandstone,  shaly 

, 5.  Coal,  blossom,  Lower  Freeport 

3a  6.  Fire  clay 

7.  Shale 

8.  Sandstone 

9.  Slate 

as’  10.  Coal,  Middle  Kittanning 

11.  Shales,  with  iron  ore  (kidney) - 

12.  Sandstone,  massive . 

f Coal blossom  1 

13.  Coal,  Lower  Kittanning  < Sandstone,  shaly  ...  7 > 

45  (Coal  blossom) 

14.  Concealed 

15.  Sandstone,  white 

16.  Shale 

17.  Iron  ore,  “ Baird,  ” buhrstone 

3 18.  Limestone,  Ferriferous 

19.  Coal  

20.  Sandstone,  white 

21.  Coal,  Clarion 

22.  Shale  

Fig.  10-.— Panther  23.  Coal,  Brookville 

Hill,  Mt.  Vernon  24.  Sandstone,  top  of  No.  XII. 

Furnace,  Scioto 
County,  Ohio. 


Feet. 

Feet. 

HI 

15  S 

38 

12  j 

20  | 

39 

4 J 

16  l 

29) 

45 

7 

8) 

6 V 

18 

4) 

blossom 


16 

blossom 


Total. 


175 


WniTE.] 


THE  LOWER  COAL  MEASURES. 


135 


Section  near  fronton,  Oliio.-^ From  the  vicinity  of  Ironton,  Ohio,  Prof. 
Orton  reports  the  following'  structure  (Fig.  109)  for  the  Lower  Goal 
Measures  (Yol.  Ill,  Ohio  Geology,  p.  928): 


Ironton,  Lawrence  County.  Ohio. 

[See  map,  R b.] 

Ft.  in.  Ft  in. 

1.  Coal,  Upper  Freeport 4 

2.  Fire  clay . 2 1 

3.  Conglomerate  and  sandstone 29 

4.  Little  yellow  kidney  or  Monitor  furnace  ore 1 

5.  Concealed 2 l Qc 

6.  Buff  limestone 2 ( 

7.  Shales 23  6 

8.  Yellow  kidney  ore  (Moxahala) 1 | 

9.  Heavy  sand  rock  . 37  6 J 

10.  Coal  No.  6 (Sheridan  coal),  Middle  Kittanning 3 

11.  Fireclay T 8 61 

12.  Black  kidney  ore 1 > 34 

13.  Sand  rock 24  6 ) 

14.  Coal  No.  V (New  Castle),  Lower  Kittanning 3 6 

15.  Fire  clay 2 ) 

16.  Sand  rock 23  6 V 31  6 

17.  Fireclay 6 ) 

18.  Limestone  ore 1 

19.  Gray  limestone,  Ferriferous 5 

20.  Sand  rock,  Hearthstone  quarries 60  6l 

21.  Conway  coal  No.  3,  C.  (Brookville) 2 > 64  6 

22.  Fireclay.. 2 ) 

23.  Top  of  No.  XII,  sandstone. 

Total 244  6 


40' 


Fig.  110.— Section 
in  southern 
Ohio,  near  Iron- 
ton. 


Section  in  southern  Ohio , near  fronton. — In  the  same 
region  of  Ironton,  but  at  a different  locality,  the  writer 
found  the  following  structure  (Fig.  110): 

In  southern  Ohio,  above  Ironton. 


[See  map,  S b.] 


1.  Coal,  Upper  Freeport 

2.  Shales  and  sandy  beds 

3.  Coal,  Lower  Freeport 

4.  Massive  sandstone 

6.  Shale 

t Coal 1'  l 

| Fire  clay 1'  | 

6.  Coal,  Middle  Kittanning. %.  ■[  Coal  V )■ 

Fire  clay 2'  | 

[Coal  2 ' ) 

7.  Fire  clay 

8.  Sandstone,  massive 

9.  Coal,  Lower  Kittanning ; 

10.  Shales  and  fire  clay  

11.  Limestone,  Ferriferous 

12.  Firti  clay  and  shales 

13.  Coal,  Clarion  

14.  Shales,  and  concealed  

15.  Massive  sandstone,  top  of  No.  XII. 

Total 


Ft.  Ft.  in. 


2 

50 

3 


7 


5* 

40  3 


45 

2 6 

25 

5 

10 

1 

40 


235  6 


This  section  differs  but  little  from  that  found  in  western  Pennsylva- 
nia. The  “Buhrstone”  or  “Baird”  ore,  which  was  not  noted  in  this, 
is  present  in  other  sections  at  its  proper  horizon  on  top  of  No.  11.  The 
Putnam  Hill,  or  lower  division  of  the  Ferriferous  limestone,  seems  to 
have  disappeared,  either  by  coalescing  with  the  upper  one  or  failure  of 
deposition,  and  the  same  appears  to  be  true  of  the  Upper  Kittanning 
coal,  unless  it  is  to  be  found  in  the  upper  layers  of  the  complex  Middle 
Kittanning  No.  G,  which  is  not  improbable. 


136 


THE  NORTHERN  BITUMINOUS  COAL  FIELD. 


[BULL.  65. 


Section  at  Charleston , West  Virginia. — As  we  leave  the  northwestern 
margin  of  the  Appalachian  field  in  southern  Ohio,  and  pass  southeast- 
ward toward  the  other  or  eastern  side  of  the  same,  the 
Lower  Coal  Measures  thicken  up  quite  rapidly,  as  will 
be  seen  from  the  line  of  sections  which  will  now  be 
given  along  the  Great  Kanawha  River.  The  following 
one  (Fig.  Ill),  from  the  mouth  of  Elk  River,  at  Charles- 
ton, is  the  record  of  Edwards  gas  well  No.  3.  It  begins 
at  the  level  of  the  Upper  Freeport  coal,  and  the  record 
was  obtained  from  Mr.  W.  S.  Edwards,  the  superintend- 
ent of  the  gas  company: 


Under  Charleston , Kanawha  County , West  Virginia,  by  bore  hole  near 
mouth  of  Elk  River. 

[See  map,  S f.] 

Ft.  in. 

1.  Coal,  Upper  Freeport 3 

2.  Shales  and  slates 55 

3.  Coal,  Lower  Freeport 1 6 

4.  Sandstone  and  shales - 116 

5.  Coal,  slaty,  Upper  Kittanning 5 

6.  Shales  and  sandstone 203 

7.  Sandstone,  coarse,  with  gas  and  water 70 

8.  Coal,  Clarion 

9.  Shales  and  sandstone 90 

10.  Shales 30 

11.  Top  ofXo.  XII,  white  sandstone. 

Total 573  6 


The  thickness  of  the  measures  is  here  about  three 
times  greater  than  in  the  Hocking  Valley,  100  miles 
north  from  Charleston.  Just  where  this  rapid  thicken- 
ing begins  has  not  ^et  been  determined,  owing  to  the 
absence  of  reliable  borings  between  the  Hocking  Valley 
and  Charleston,  but  it  is  probable  that  the  most  of  it 
comes  in  from  the  Ohio  River  southward  to  Charleston, 
since  the  borings  at  Pomeroy  and  Hartford  City  disclose 
no  unusual  thickness  of  the  Lower  Coal  Measures. 

The  identification  of  coal  No.  8 in  the  above  section  is 
open  to  question,  as  it  may  possibly  represent  the  Lower 
Kittanning  bed. 

There  may  have  been  other  bedsof  coal  passed  through 
by  the  drill  in  the  well  from  which  this  section  is  taken, 
since  it  is  seldom  that  drillers  for  oil  and  gas  exercise  much  care  in  ex- 
amining the  drillings  for  coal. 


Fio.  111. — Section 
under  Charles- 
ton, W.  Va. 


WHITE.] 


THE  LOWER  COAL  MEASURES. 


137 


Section  at  mouth  of  Lick  Run,  near  Charleston , West  Virginia . — Neur 
the  mouth  of  Lick  Run,  2 miles  south  of  Charleston,  a well  was 
bored  for  gas,  by  Mr  Hulings,  and  from  the  super- 
intendent, Colonel  Jordan,  I obtained  the  following 
52’  record  (Fig.  112)  by  combining  it  with  the  70  odd 
feet  of  rocks  exposed  above  the  mouth  of  the  bor- 
ing: 

,,  - 

eo’  At  mouth  of  Lick  Bun,  two  miles  eCbme  Charleston , Kanawha 
County,  West  Virginia. 


245* 


195 


Fin.  112.— month 
of  Lick  Run,  two 
miles  above  Charles- 
ton, W.Va. 


[See  map,  T f.] 


Feet. 


1.  Coal,  Upper  Freeport 

2.  Shales 

3. 

4. 

5. 


Concealed 

Sandstone, massive  ... 
Coal,  Lower  Freeport . 
Shales  and  concealed 
Blue  slate 


7 I 

20  y 

25  1 


( Blue  sandstone,  hard . . 51/  ] 
j Slate  and  sandstone. ..  6'  j 

Sandstone,  Freeport  { Sandstone,  hard 73'  > . . . . 

| Slate 21'  I 

1 Sandstone,  hard 94'  j 


:i 


Slate,  blue 

Sandstone 


Slate 

Sandstone,  white 

Sandy  shale,  dark  blue 

White  pebbly  sandstone,  top  of  No.  XII. 
Total 


Feet. 

3 

52 

3 

€0 

245 

33 

50 

32 

15 

195 


Colonel  Jordan  states  that  no  particular  search 
was  made  for  coal  here,  and  hence  several  beds  may 
have  been  passed  unnoticed.  It  is  also  possible  that 
the  top  of  No.  XII  is  placed  about  100  feet  too  low 
by  the  section  above,  since  the  ordinary  driller  fre- 
quently neglects  to  note  changes  in  the  character  of 
the  strata  through  which  the  drill  passes;  hence  it 
is  quite  probable  that  a considerable  thickness  of  No. 
13,  which  the  drillers  called  u sandy  shale,”  may  have 
been  really  the  top  portion  of  the  No.  XII  series. 

The  Freeport  sandstone,  No.  8,  exhibits  an  unusual 
development  here,  and  it  is  possible  that  the  lowest 
division  included  in  No.  8 is  not  really  a member  of 
this  stratum,  but  belongs  lower  in  the  series. 

No.  10  is  probably  a representative  of  the  Kittan- 
ning sandstone. 


138 


THE  NORTHERN  BITUMINOUS  COAL  FIELD. 


[BULL.  G5. 


Section  at  Dickinson  salt  works , Kan  ay  ha  County , West  Virginia. — 
In  the  vicinity  of  Malden,  6 miles  above-  Charleston,  the  rapid  rise  of 
the  strata  on  the  northwestern  slope  of  the  Brown stown  anticlinal  has 


brought  nearly  all  of  the  Lower  Coal  Measures  to 
the  surface,  and  the  rest  of  the  column  is  supplied 
from  the  records  of  the  Edwards  gas  well  No.  2,  at 
the  Dickinson  salt  works.  The  combined  section 
reads  as  follows  (Fig.  113): 


Dickinson  salt  works , Kanawha  County , W st  Virginia. 


[See  map,  T f.J 

1.  Coal,  Upper  Freeport,  slaty 

2.  Shales 

3.  Sandstone,  massive 

4.  Shales 


5.  Coal,  Lower  Freeport.. 


6^  Shales 

7.  Sandstone,  massive 

8.  Sandy  shales,  with  iron  ore  nodules . 

9.  Concealed 

10.  Sandstone,  massive 

C Coal,  slaty O'  5"  ) 

11.  Coal,  Upper  Kittanning  < Slate,  black 0'  11"  > 

■ (Coal 2'  1") 

12.  Fire  clay,  sandy 

13.  Concealed * 

14.  Sandstone,  massive 

it;  rw  5 Cedar  Grove ( 

Coal \ Middle  Kittanning 5 

16.  Concealed,  and  shales 

17.  Sandstone 

18.  Sandy  shales 

19.  Limestone,  siliceous,  Campbell’s  Creek 

20.  Shales  and  sandstone 


21.  Coal,  Campbell’s  Creek, 
Lower  Kittanning . . . 


22.  Shales 

23.  Sandstone,  massive 

24.  Concealed  in  bore  hole 

25.  Sandstone,  white 

26.  Shales 

27.  White  sandstone,  top  of  Ko.  XII.  ' 


( Coal 2'  0") 

Shales 1'  2" 

Coal 0'  4" 

Fire  clay  and  shales  1'  10" 
Coal  and  slate O'  8" 


Coal O'  10" 

1 Slate 0'  2" 

Coal V 8" 

j Fire  clay  and  shales  7'  0" 

Coal,  slaty 0'  6" 

I Fire  clay 1'  2" 

[Coal (f  3" J 


( Cedar  Grove 

} Middle  Kittanning. 


( Coal,  slaty 1'  6" 

I Rock O'  6" 

{ Coal 1'  6" 

| Shale 0'  6" 

[Coal,  slaty 1'  6" 


ore  nodules 


Ft.  Ft.  in. 
4 
5 

65  S 85 
15 


5} 

65 

3 

20 
50  j 


143 


2? 

55  V 187 
130  ) 


151 

it 

35 


0 8 


63 


17  7 


SI 


132 


Total. 


641  2 


This  section  would  seem  to  confirm  the  statement 
made  in  connection  with  the  Lick  Run  boriug,  viz, 
that  a part  of  the  last  interval  given  there  should 
more  properly  be  credited  to  No.  XII,  the  next 
series  below  the  Lower  Coal  Measures. 

The  Campbell’s  Creek,  or  Lower  Kittanning  coal, 
is  here  very  much  split  up  with  slate  and  shales, 


fig.  113. — Sec ti o n at  but  on  the  Malden  side  of  the  Kanawha  it  is  a good 
KanaTha  County^wl  bed,  from  which  4 to  6 feet  of  coal  is  obtained  with 

Va  ‘ 

only  the  two  parting  slates. 

This  is  the  type  locality  of  the  Campbell’s  Creek  limestone  No.  19. 


WHITE.] 


THE  LOWER  COAL  MEASURES. 


139 


Section  near  Brownstown , West  Virginia. — In  rthe  vicinity  of  Browns* 
town  and  near  the  Burning  Spring,  9 miles  ^^e^Gharleston,  another 
gas  well  was  drilled  (Edwards  No.  1)  and  its  record 
combined  with  the  surface  exposures  in  that  vicinity 
gives  the  following  succession  (Fig.  114) : 


Near  Broivnstoicn,  three  miles  south  from  Malden. 


[See  map,  T f.] 


<37^ 


2'  6" 


1.  Coal,  Upper  Freeport,  slaty 

2.  Concealed 

3.  Sandstone,  massive,  gray 

4.  Shales,  and  concealed 

5.  Sandstone,  massive,  gray 

6.  Sandy  shales,  and  concealed 

7.  >andstone,  gray,  micaceous 

8.  Concealed 

9.  Coal  (Cedar  Grove),  Middle  Kittanning. 

10.  Concealed,  and  sandstone 

( Lower  Kit-  1 Coal 

12.  Coal.  < > Shales  and  sandstone  ..20'  0" 

j Campbell  s f Pnal  9, 

[ Creek.  J Coal Z 4 

13.  Shales - 

14.  Sandstone,  massive 

15.  Concealed *. 

16.  Coaly  shale 

17.  Fire  clay,  sandstone,  and  concealed 

18.  Coal,  Brownstown 

19.  Shales 

20.  Sandstone,  massive 

21.  Sandy  shales  and  flaggy  sandstone 

22.  Limestone,  siliceous,  Ferriferous 

23  Shales,  sandy 

24.  Slate,  black. 

25.  Shales 

26.  Sandstone,  and  concealed 

27.  Coal,  Clarion  (Eagle) 

28.  Sandstone 

29.  Slate,  gray 

30.  Sandstone,  gray  

31.  Slate,  dark  

32.  White  sandstone,  top  of  No.  XII. 


It.  in. 

10 

95 

30 

40 

25 

160 

15 


Ft.  in. 
5 


)>  375 


Total .. 


3 4 

100 

24  10 

74 

2 

70 

1 

45  6 

3 


801  8 


100 


741 


The  only  part  of  this  series  dependent  on  the  bore 
hole  record  is  the  last  100  feet,  or  that  from  the 
Clarion  coal  down,  the  rest  of  it  all  being  exposed 
above  the  bed  of  the  Kanawha  in  the 
region  of  Brownstown. 

By  comparing  this  with  the  Charles- 
ton section  (Fig.  Ill)  it  will  be  seen 
that  the  whole  column  has  thickened 
southward  at  the  rate  of  about  25  feet 
to  the  mile.  It  will  also  be  observed 
that  with  this  thickening  a new  coal, 
the  Brownstown,  makes  its  appear- 
ance in  the  series.  This  is  one  of  a 
local  group  of  two  or  three  coals  which 
appear  in  the  column  of  rocks  around 
the  southeastern  margin  of  the  coa 
field  between  the  Lower  Kittanning  bed  and  the  Ferriferous  limestone, 
which  would  seem  to  be  represented  by  No.  22  of  the  section.  These  coals 
are  of  little  economic  importance,  as  they  are  usually  thin  and  slaty. 


Fig.  114. — Section  near  Brownstown,  three 
miles  south  from  Malden,  W.  Va. 


140 


THE  NORTHERN  BITUMINOUS  COAL  FIELD. 


[BULL.  G5. 


Section  at  mouth  of  Armstrong  Creek,  on  the  Big  Kanawha  River , West 
Virginia.— At  the  mouth  of  Armstrong  Creek,  25  miles  south  from 
Charleston,  the  whole  column  of  the  Lower  Coal  Measures  is  above 
water  level,  and  a high  point  almost  vertically  above 
the  Kanawha  Kiver  catches  the  top  members  of  the 
same,  so  that  here  a very  fine  exposure  of  the  series 
gives  the  following  structure  (Fig.  115) : 

Mouth  of  Armstrong  Creek,  on  the  Big  Kanawha  River. 

[See  map,  U g.]  Ft. 

1.  Coal.  Upper  Freeport 

2.  Sandstone,  and  concealed 170' 

3.  Sandstone,  massive 60 

4.  Concealed,  and  sandstone 115 

5.  Limestone,  siliceous  2 


zo' 


zhr 


--  — - 

BrCTftyCWSBBBp' 


Ft.  in. 
3 


372 


Coal 

...  6" 

Shale... 

...  8" 

Coal.  — 

...  5" 

Shale 

...  6" 

Coal 

...  4" 

2 5 


8.  Fire  clay,  and  concealed. 

9.  Sandstone,  massive . 


5] 

20 


37i'  10.  Shales,  concealed,  and  sandstone 20 

20 


11.  Concealed, 

12.  Sandstone  and  shales 20  >165 

13.  Sandstone,  massive 25  J 

14.  Shales,  and  concealed 20  I 

15.  Sandstone 25  | 


H 

6"  ) 


V 8" 


0"  | 
0"  I 

0"  I 

5"  f 
i"  C 


16.  Sandy  shales 

Coal 1' 

Slate 0' 

Coal O' 

Sandy  shales 12' 

Coal,  “ Peerless  ” 2' 

. Shales,  bluish. 15' 

17.  Coal,  Lower  Eittan-  \ Coal,  sulphurous O' 

ning \ Slate 0' 

Coal 0'  6" 

Coal,  splint O'  11" 

Parting O'  £" 

I Coal 0'  7"  I 

| Slate O'  I 

[ Coal 2'  10"  J 

18.  Fireclay - 

19.  Sandstone  and  shales . 

[Coal V 0"1 

Shale 2'  6"  | 

20.  Coal,  Browns-  ! Coal O'  10" 

town ] Shales  and 

sandstone  . .15'  0" 

1 Coal 1'  2" 


10J 


z°' 


l2'6foS| 

15’ 

ft" 


40’ 


36 


21.  Concealed,  and  sandy  shales. 40  ) 

22.  Limestone,  siliceous,  Ferriferous 1 > 

23.  Shales 10) 

Coal 0'  8"] 

Shales 1' 

Coal,  slaty  ...  0' 


20  6 


51 


24.  Coal,  Clarion 


< Shales,  sandy. 20' 
<Ea*le> | Coal..........  0' 


" 

:: 


I Shales 0'  8"  I 

[Coal 2'  10"  J 

25.  Shales  and  sandy  beds 

26.  Coal.  Little  Eagle - 

27.  Fire  clay  and  shales 


I3l' 


30.  Limestone,  fossiliferous,  Eagle  . . . 

31.  Dark  shales,  fossiliferous  . . 

32.  Shales,  sandstones,  and  concealed. 

33.  Bituminous  shale 


35.  Limestone,  siliceous •>.. 

36.  Shales,  sandstone,  and  concealed r-.. 

37.  Sandstone,  massive,  top  of  No.  XII. 


26 

20 

- 51 

1 

1° 

> 55 

40 : 

1 

1 

5 ] 
75  J 

> 80 

2 

30  ) 

l 

1 

»131 

ioo  5 

I-  ‘ 

Total. 


1,  006  7 


Fig.  115. — Section  at  mouth  of  Armstrong 
Creek,  en  the  Big  Kanawha  Uiver. 


WHITE.] 


THE  LOWER  COAL  MEASURES. 


141 


Here  both  the  Lower  Kittanning  and  the  Clarion  coals  show  in  their 
structure  the  eifect  of  the  general  thickening  up  of  the  whole  column 
of  rocks.  Three  miles  north  from  this,  the  Clarion  or  Eagle  coal  is  a 
good  bed,  which,  with  its  partings  of  slate,  is  only  4J  feet  thick,  but  the 
partings  gradually  thicken  and  new  ones  come  in  till  the  structure 
shown  in  No.  24  is  obtained. 

A small  coal  which  has  been  termed  the  Little  Eagle  comes  into  the 
section  in  this  region,  and  seems  to  have  a wide  distribution  around 
the  southern  margin  of  the  coal  field.  It  is  a very  pure  coal  and  may 
be  a lower  member  of  the  Clarion  bed. 

The  Eagle  limestone,  No.  30,  was  named  from  a mining  village  3 
miles  below  the  locality  of  this  section,  where  it  is  finely  exposed  in  the 
cuts  of  the  Chesapeake  and  Ohio  Railroad.  It  and  the  shales  below  it 
are  crowded  with  the  Lower  Coal  Measures  fossils,  the  general  facies  of 
the  fauna  being  very  similar  to  that  found  in  connection  with  the  Fer- 
riferous limestone  in  western  Pennsylvania,  but  the  general  section  for- 
bids the  supposition  that  it  is  identical  with  the  latter.  At  one  time  I 
entertained  the  idea  that  it  might  be  the  representative  of  the  Putnam 
Hill  limestone,  of  Ohio,  but  a closer  study  of  the  Ohio  section  renders 
that  hypothesis  untenable,  since  the  Putnam  Hill  bed  belongs  above 
the  Clarion  coal  and  not  below,  as  does  the  Eagle  limestone. 

No.  33  is  a very  bituminous  shale,  since  lubricating  oil  was  once 
manufactured  therefrom,  and  it  may  possibly  represent  the  Brookville 
coal  of  Pennsylvania. 

A comparison  of  this  section  with  those  on  the  other  side  of  the  Ap- 
palachian basin  at  Buchtel  (106)  and  Shawnee  (105)  will  show  the 
wonderful  expansion  of  these  beds  from  175  feet  at  the  latter  localities 
to  a thickness  of  more  than  1,000  feet  at  Armstrong’s  Creek,  and  the 
same  thing  is  shown  graphically  in  map,  Section  C.  That  such  a great 
expansion  of  these  measures  should  show  only  the  same  number  of 
workable  coal  beds  as  the  section  at  Shawnee  was  hardly  to  be  expected, 
but  it  is  true  beyond  question.  The  coal  beds  themselves  give  evidence 
of  this  great  expansion  of  the  general  column  in  the  slates  and  other 
impurities  with  which  they  are  interstratified. 

The  interval  (165  feet)  which  here  separates  the  Middle  and  Lower 
Kittanniug  coal  beds  appears  excessive,  since  it  is  only  100  feet  a few 
miles  below,  but  there  can  be  very  little  doubt  of  the  figures  given,  and 
as  there  are  no  coal  beds  between  Nos.  7 and  17,  it  is  evident  that  No. 
7 must  be  the  Middle  Kittanniug. 

The  top  member  of  the  Pottsville  conglomerate  is  in  the  bed  of  the 
Kanawha,  where  the  section  shown  in  Fig.  115  ends. 


142 


THE  NORTHERN  BITUMINOUS  COAL  FIELD. 


[BULL.  65. 


Section  at  Guyandotte  Mountain , Raleigh  County , West  Virginia. — 
That  the  Lower  Coal  Measures  keep  their  greatly  expanded  measure- 
ment on  south  westward  from  the  Kanawha  River  is  shown  by  the  fol- 
lowing section  (Fig.  116)  made  by  Captain  Miller,  chief  engineer  of  the 
Trans-Flat-Top  Land  Association.  It  begins  at  the  summit  of  Guy- 
andotte Mountain,  Raleigh  County,  West  Virginia, 
and  was  measured  along  the  turnpike  eastward  to  the 
foot  of  the  mountain  : 


Guyandotte  Mountain , Raleigh  County , West  Virginia. 


[See  map,  W g.] 


1.  Upper  Freeport  coal  (absent). 

2.  Massive  sandstone 

3.  Shales 


4.  Coal,  Lower  Freeport . . ^ Slate 

5.  Shale 


6.  Coal,  Winnifrede Slate 


( Coal 

< Slate 

L Coal 

3'  10"  i 

. 0'  1"> 

O'  9") 

{ Coal  

2' 

5") 

1 Shale 

12' 

2"  1 

| Coal 

1' 

3"  1 

Slate 

0' 

2"  )■ 

1 Coal 

2' 

3''  1 

! Slate 

O' 

1"  ! 

[Coal 

O' 

1"J 

Ft.  in.  Ft.  in. 

83 

15 


7.  Sandstone,  hard,  gray 28 

8.  Shale  81 

9.  Sandstone 8 

10.  Shale 14 

11.  Sandstone,  hard,  grav 53 

12.  Shale .1 32 

13.  Sandstone,  shaly 24 

14.  Shale,  yellowish 7 


247' 


Coal 

0'  7 " 

Slate  

0'  1 " 

Coal 

0'  9 " 

Slate  

0'  0*" 

Coal 

1'  1 " 1 

Slate  

0'  4 " 1 

Coal 

v H"J 

67 


16.  Sandstone,  soft,  yellow 19 

17.  Coal 0 

18.  Fireclay 1 

19.  Shales,  yellowish 36 


21/ 


20.  Coal,  Browns* 
town 


70 


26' 


f Coal O'  1' 

< Fireclay.  2'  0' 
(Coal...'..  1'  1") 

21.  Fire  clay 0 

22.  Sandstone,  soft,  yellow 15 

23.  Sandstone,  hard,  gray 22 

24.  Sandstone, soft, yellow, micaceous  21 

25.  Shales,  yellowish 67 

26.  Coal  0 

27.  Fire  clay 1 

28.  Slate,  black 16 

29.  Sandstone,  soft,  yellow 35 

30.  Shales,  yellow  39 


31.  Coal,  Eagle 


ZO& 


[Coal 

1'  3" 

Slate  

4'  0" 

Fire  clay  . . 

2'  0" 

Coal 

0'  1" 

Clay 

0'  3" 

Coal 

0'  9" 

Clay 

0'  2" 

Coal 

0'  1" 

Clay 

1'  0" 

[Coal 

0'  1" 

Fig.  116. — Section  at  Gnyandotte  Mountain, 
Raleigh  County,  W.  Va. 


32.  Sandstone,  hard,  gray 13 

33.  Sandstone,  soft,  yellow 33 

34.  Coal,  Little  Eagle 

35.  Fireclay 1 

36.  Shales,  sandy,  yellow 46 

37.  Sandstone,  soft,  yellow 70 

38.  Shales,  sandy,  yellowish 58 

39.  Sandstone,  flaggy 7 

40.  Shales,  yeilow 26 

41.  Pebbly  sandstone,  top  of  Xo.  XII. 


4 8 
43 


18  5 


247 


1 

56  3 

“j 

3 2 


2 \ 217 

4 . 


0 8 


0 3 


Total. 


>2u8 


855  5 


WHITE.  J 


THE  LOWER.  COAL  MEASURES. 


143 


It  is  possible  that  the  horizon  of  the  Upper  Freeport  coal  should  have 
been  placed  higher  than  the  section  shows,  since  the  coal  is  not  present 
and  the  place  given  it  is  only  a surmise. 

Section  near  Oceana , Wyoming  County , West  Virginia. — In  the  vicinity 
of  Oceana,  Wyoming  County,  West  Virginia,  and  the  neighboring  re- 
gion, the  Lower  Coal  Measures  present  the  following 
structure  (Fig.  117): 

Wyoming  County , West  Virginia. 


[See  map,  W f.] 


1.  Upper  Freeport  coal  (not  seen) 

2.  Sandstone,  and  concealed  . 

( Coal 


Ft.  in. 


O' 


\\v 


■ *.*■■*  *->  - 


* ♦ ♦ r * • 


3.  Coal,  Lower  Freeport . . 


1" 

Shale O'  4" 

Coal 0'  10"  . 

Bony  coal 0'  4"  | 

Coal 2'  l".j 


4 Sandstone,  and  concealed  

5.  Cannel  slate  mixed  with  coal,  Upper  Kittanning. 

6.  Concealed „ 

7.  Sandstone,  massive 


15S1 


8.  Coal,  Middle  Kit- 
tanning  


( Coal 

1' 

6"  ) 

< Shale 

0' 

5"  > 2 

(Coal 

0' 

8"  5 

Shales  and  sandstone 

20 

^ f Coal,  good 

2' 

6"  ) 

1 Shale,  gray 

0' 

2*" 

i Coal 

0' 

34"  > 4 

| Shale,  gray 

0' 

10"  I 

1 [Coal 

0' 

9"  J 

fe'a’ 


100* 


n'2? 


wa11 


2 A$* 


40 


ZO 

7V 


9.  Concealed,  and  sandstone 20 

10.  Coal 0 

11.  Fire  clay  and  shales 5 

12.  Sandstone,  massive 50 

13.  Shales,  dark,  slaty 10 

Coal..  1'  0") 
Slate.  10' 

Coal..  1' 

Slate, 

dark. 

Coal . . 

Slate  . 

I Coal . . 

I Slate  . 

I Coal . . 

15.  Massive  sandstone  ... 

16.  Concealed 40 

17.  Shales 20 


tfitf 


7Q 


5 ft 


65’ 


14.  Coal,  Lower 
Kittan- 
ning 


O' 

8" 

0'  6" 

V 2"  f 
0'  4"  | 
4'  0" 

5'  3"  I 
0'  10" J 


100 


2d 


18.  Coal,  Browns- 


20. 


Coal,  Eagle 
(Clarion) 


f Coal.. 

. 1'  7" 

Slate . 

. 1'  4" 

Coal.. 

. 0'  2" 

Q 1 Sla  te . 

. 0'  8" 

8'-»  Coal.. 

. 0'  4"  ; 

’ ' 1 Slate  . 

. 0'  4"  | 

Coal.. 

. 0'  6" 

1 Slate . 

. 1'  8"  | 

1 Coal. . 

. 1'  0"  J 

and  concealed  . . 

C Coal . 

. 3'  4"  ) 

< Slate . 

. 0'  4"  ) 

•’  (Coal.. 

. 2'  0"  j 

21.  Concealed,  and  shales 

22.  Coal,  Little  Eagle 

23.  Shales  and  sandstones 75 

24.  Shales,  gray,  with  fossil  plants  5 

25.  Coal 

26.  Concealed, and  shales  and  sand- 

stone   

27.  Coal,  blossom 

28.  Shales 

29.  Massive  sandstones,  top  of 

No.  XII. 


Total 


bmmm 

Fig,  117.— Section  near  Oceana,  Wyoming 
County,  W.  Va. 


Ft.  in. 
100 


155 

3 

2 

70 


> 27  2 


24  9 


160 


7 7 


10 


100 

30 


993 


144 


THE  NORTHERN  BITUMINOUS  COAL  FIELD. 


| BULL.  65. 


No.  20  is  known  as  the  “coking  coal  ” in  the  Wyoming  region,  since 
it  has  the  typical  structure  of  such  coal,  and  looks  very  much  like  the 
same  (Eagle)  bed  on  the  Kanawha. 

The  Little  Eagle  bed  No.  22  is  also  very  good  coal  here,  and  its  in- 
terval below  the  main  seam  has  increased  from  20  to  05  feet. 

Section  at  mouth  of  Blaine  Greek , Lawrence  County , Kentucky. — In 
passing  southward  up  the  Big  Sandy  River,  at  the 
southwestern  line  of  West  Virginia,  the  Lower  Coal 
Measures  thicken  up  at  about  the  same  rate  as  they 
do  along  the  Kanawha,  as  will  be  seen  from  the  follow- 
ing sections.  The  first  one  (Fig.  11 8)  is  from  a sur- 
face measurement,  combined  with  the  record  of  liig- 
don  gas  well  No.  2,  at  the  mouth  of  Blaine  Creek,  JO 
miles  above  the  mouth  of  the  Big  Sandy  River,  and 
reads  as  follows : 


122,* 


Mouth  of  Blaine  Creelc,  twenty  miles  above  mouth  of  Big  Sandy 
Biver,  Kentucky. 


[See  map,  T b.] 


Fig.  118. — Section  at 
mouth  of  Blaine 
Creek,  Ky. 


1.  Coal  and  black  slate,  Upper  Freeport 

2.  Sandstone 

3.  Slate,  black 

4.  Coal,  Lower  Freeport 

5.  Fireclay 

6.  Sandstone,  white 

7.  Sandstone,  dark  gray 

8.  Sandstone,  white 

9.  Slate,  black 

10.  Sandstone,  dark 

11.  Slate,  black 

12.  Coal,  Middle  Kittanning 

13.  Slate 

14.  Sandstone,  gray 

15.  Slate,  black 

16.  Sandstone,  gray 

17.  Coal,  Lower  Kittanning 

18.  Fire  clay 

19.  Sandstone,  gray 

20.  Slate,  gray 

21.  Sandstone,  gray 

22.  Slate,  black 

23.  Sandstone,  white,  top  of  No.  XII. 


Feet.  Feet. 

5 

30  > 

50  ( 80 

4 
7 

45 
10 
10 
15 
25 
10 

27 


122 


25 


Total. 


218 


521 


For  the  carefully  kept  record  of  this  boring  I am  indebted  to  Mr. 
F.  H.  Oliphant,  now  the  chief  geologist  of  the  South  Penn  Oil  Com- 
pany. 


WHITE.] 


THE  LOWER  COAL  MEASURES. 


145 


Section  near  Old  Peach  Orchard , Laivrence  County , Kentucky. — Id  the 
vicinity  of  Old  Peach  Orchard,  on  the  Louisa  fork  of  Big  Sandy 
Biver,  Kentucky,  the  surface  measurements,  com- 
bined with  the  records  of  oil  and  gas  borings  near  by, 
give  the  following  structure  (Fig.  119) : 


1:1 


15' 


SM4' 

35* 


Near  Peach  Orchard,  Kentucky. 

[See  map,  V b.J 


Ft.  in.  Ft.  in. 


Upper  Freeport  coal  (absent) 

Sandy  shales - 20 

Sandstone  and  sandy  beds 80 


Coal 


f Lower  Freeport,  or  | 

r Coal  — 

...O' 

10"  ) 

< Winnifrede,  Peach  < 

; Shale  ... 

...  0' 

10"  J 

( Orchard  bed- 1 

[Coal  .... 

...  2' 

4"  ) 

100 

< 


> 137  4 


15.  Coal 


>") 

S">— • 

V'S 


4| 


Fire  clay,  siliceous 2 

Sandy  shales  35 

Massive  sandstone  and  sbaly  micaceous  beds 75 

Blue  sandy  shales - : 25 

( Cannel 1'  0" 

Coal,  Upper  Kittanning<  Clay  O'  6" 

t Coal,  slaty 1'  0" 

Shale  and  sandstone 10 

Coal  - 0 

Sandy  shale,  blue 8 

Limestone 2 

Sandstone,  shaly 12 

( Coal O'  6"  ) 

< Shale 1'  6"  V .... 

( Coal O'  8"  ) 

16.  Concealed,  and  shaly  sandstone 9 

17.  Black  slate  4 

18.  Coal,  splint,  Middle  Kittanning 

19.  Concealed  10 

20.  Hard  sandstone 70 

21.  Blue  shale 2 

22.  C<  al,  Lower  Kittanning 

23.  Shales  and  fire  clay 10 

24.  Sandy  shale 15 

25.  Black  shales 115 

26.  Sandstone 4 

27.  Dark  shale 110 

28.  White  sandstone,  top  of  No.  XII. 

Total 634  10 


r* 


2 6 
32  4 

2 8 

13 

1 

82 

6 

254 


The  place  of  the  Upper  Freeport  coal  here  is  deter- 
mined with  comparative  certainty  by  the  massive  Ma- 
honing sandstones,  which  come  in  above  No.  1,  and 
also  by  the  occurrence  of  the  Mahoning  coal,  with  its 
characteristic  structure,  at  235  feet  above  the  Peach 
Orchard  bed,  and  135  feet  above  where  the  horizon  of 
the  Upper  Freeport  has  been  placed. 

No.  15  is  very  probably  a “split”  from  the  Middle 
Kittanning  bed,  No.  18,  and  should  be  regarded  as 
a part  of  the  latter. 

The  Lower  Kittanning  bed,  No.  22,  is  given  as  re- 
ported from  a bore  hole  at  “ Old”  Peach  Orchard,  by 
Prof.  Shumard,  who  examined  the  drillings  at  the 
time  the  boring  was  made,  and  the  rest  of  the  section 
FoVd19  T>SeacbD  ()?■  below  this  is  from  a deep  boring  made  for  gas,  about 
3 miles  distant,  the  record  of  which  was  obtained  from 
Mr.  F.  H.  Oliphant,  the  civil  engineer  under  whose  superintendence 
the  deep  well  was  bored. 

Bull  65 10 


146 


THE  NORTHERN  BITUMINOUS  COAL  FIELD. 


[BULL.  65. 


There  has  been  much  variance  of  opinion  among  geologists  who  have 
examined  the  Peach  Orchard  coal  bed  as  to  its  horizon  in  the  series, 
some  placing  it  as  far  down  in  the  column  as  the  Clarion  coal,  but  this  sec- 
tion shows  that  it  is  either  the  Lower  Freeport  coal  of  the  Pennsylvania 
column  or  else  one  that  is  probably  a u split”  from  the 
latter,  viz,  the  Winnifrede  bed  of  the  Kanawha  series. 

Section  near  Warfield , Kentucky. — In  the  vicinity  of 
Warfield,  Kentucky,  opposite  the  line  of  Logan  County, 
West  Virginia,  and  60  miles  above  the  mouth  of  the  Big 
Sandy,  the  following  structure  (Fig.  120)  is  obtained  by 
combining  the  surface  observations  with  the  records  of 
of  the  Warfield  gas  wells : 

Warfield,  Kentucky,  on  Tug  Fork  of  Big  Sandy  Biver. 

[See  map,  V b.l 


«/ 


Upper  Freeport  coal  (not  seen) . 
Massive  sandstone,  and  concealed 


sa' 


3.  Coal,  Winnifrede... 


f Coal 

. O' 

5"  1 

1 Sandy  shales. . 

.10' 

0"  1 

| Fire  clav 

. 2' 

0" 

j Coal,  splint 

. 1' 

2"  [ 

i Clay 

. 0' 

1 "l 

1 Coal,  splint 

. 1' 

4" 

1 Clay 

. 0' 

i"\ 

[Coal 

. 0' 

9"  J 

Ft.  in.  Ft.  in. 
150 


15  0 


4.  Concealed,  and  sandstone 25 

5.  Limestone,  siliceous 4 

6.  Shales,  sandstone,  and  concealed 30 

7.  Coal,  cannel,  Upper  Kittanning 

8.  Sandstone,  and  concealed 30 

9.  Limestone,  siliceous  I 

10.  Sandstone,  and  concealed 20 

11.  Coal,  blossom,  Middle  Kittanning 

12.  Concealed,  and  sandstone 

13.  Limestone,  siliceous 

14.  Sandstone,  massive 20 

15.  Shale 0 

16.  Coal 0 

17.  Sandstone  and  shales 40 

18.  Sandstone,  massive 10 

( Coal O'  4"  > 

19.  Coal,  Lower  Kittanning  < Shale O'  10"  v 

( Coal 4'  0"  S 

20.  Concealed,  and  sandstone 

21.  Limestone,  siliceous 

22.  Shales  and  sandstones  to  top  of  Xo.  XU 

Total 


45 

2 

320 

787  6 


Some  have  supposed  that  No.  3 of  this  last  section  is 
identical  with  the  Peach  Orchard  bed,  but  it  seems  to 
occupy  a horizon  a few  feet  below  the  latter,  and  I have 
therefore  referred  it  to  the  Winnifrede  bed 
of  the  Kanawha  column. 

No.  19,  which  is  locally  known  as  the 
“ Warfield”  coal,  is  the  same  one  as  No.  22 
of  Section  119,  and  the  representative  of  the 
Lower  Kittanning  bed. 

The  u siliceous”  limestones,  Nos.  13  and 
21,  may  possibly  represent  the  Campbell’s 
Creek  and  Ferriferous  beds  respectively. 


Fig.  120. — Section  at  Warfield,  Ky., 
on  Tug  Fork  of  Big  Sandy  Biver. 


WHITE. J 


THE  LOWER  COAL  MEASURES. 


147 


Section  on  Tut/ Fork  of  Big  Sandy  River , Logan  County , West  Virginia. — 
^Near  the  mouth  of  Kuox  Creek,  at  the  southern  edge  of  Logan  County, 
50  miles  by  the  river  above  Warfield,  the  following  section 
(Fig.  121)  was  constructed  on  the  West  Virginia  side  of 
Tug  River,  by  adding  to  the  upper  portion  of  the  section 
there  the  part  which  has  been  removed  by  erosion: 


300* 


m 


100' 


Tug  Fork  of  Big  Sandy  River , near  mouth  of  Knox  Creek , southern  edge 
of  Logan  County,  West  Virginia. 


' 5sT 


vvTvavN' 


40' 


tao’ 


[See  map,W  d.J 

1.  Upper  Freeport  coal  (absent) 

2.  Shales  and  sandstone 

3.  Coal,  Lower  Freeport 

4.  Shales  and  massive  sandstone 

5.  Coal,  Lower  Kittanning,  large  blossom 

6.  Sandstone,  massive 

7.  Shales,  sandstone,  and  concealed 

8.  Coal,  Eagle,  large  blossom 

9.  Shales  and  sandstone 

10.  Coal,  blossom,  Little  Eagle 

11.  Concealed 

12.  Sandstone,  flaggy 

13.  Concealed 

14.  Sandstone,  gray 

15.  Shales,  soft,  gray 

16.  Limestone,  blue,  impure  (Eagle?) 

17.  Shales,  dark  blue 

18.  Sandstone 

19.  Concealed 

20.  Coal 

21.  Shales  and  flaggy  sandstone 

22.  Slates,  dark 

23.  Concealed,  sandstone,  and  concealed 

24.  Massive  coarse  sandstone,  top  of  No.  XII. 

Total 


Ft. 


5(f 


7 ZS' 


Ft. 

100 

300 

6 

40 

180 

5 

55 

2 

140 

1 

75 

l 

85 


Wflf 


CHARACTERISTIC  HORIZONS. 

THE  UPPER  FREEPORT  COAL. 


Asmaybeseen  by  the  sections  just  given, 
a very  important  coal  bed  comes  at  the 
summit  of  the  Lower  Coal  Measures  column, 
and  marks  the  latter  off*  from  the  Barrens 
above.  This  coal,  which  was  named  the 
Upper  Freeport  coal  by  Rogers,  has  a very 
wide  distribution  in  the  Appalachian  field 
and  is  the  source  of  much  valuable  coal 
and  coke.  The  coal  is  not  entirely  persist- 
ent, however,  being  frequently  too  thin  to 
mine,  and  from  large  areas  it  is  absent  en- 
tirely, though  its  horizon  in  the  measures 
can  then  still  be  determined,  and  generally  without  much  difficulty. 
The  bed  is  probably  more  regular  and  persistent  in  Pennsylvania  than 


Fig.  121.— Section  on  Tug  Fork  of  Big 
Sandy  River,  near  mouth  of  Knox 
Creek,  southern  edge  of  Logau  Coun- 
ty, W.  Va. 


148 


. THE  NORTHERN  BITUMINOUS  COAL  FIELD 


[BULL.  65. 


in  either  of  the  other  two  States  (Ohio  and  West  Virginia),  but  even 
there  it  is  not  always  found  in  workable  condition,  being  thin  or  want- 
ing in  some  portions  of  nearly  every  county  where  its  outcrop  extends. 

One  of  the  main  features  which  characterizes  this  bed  is  its  complex- 
ity, since  it  is  always  separated  into  two  or  more  benches  by  divisions 
of  slate.  This  complexity  of  structure  is  illustrated  at  the  type  locality 
(Section  G6),  and  so  far  as  the  writer  knows  it  is  never  entirely  absent 
anywhere  in  the  Appalachian  field,  whenever  the  bed  is  thick  enough 
to  mine.  These  parting  slates  vary  in  both  number  and  thickness  in 
different  regions,  so  that  there  is  nothing  characteristic  about  them  over 
the  whole  field,  but  yet  in  any  particular  district  or  coal  basin  their 
number  and  position  in  the  bed  are  quite  regular. 

Another  peculiarity  of  the  coal  is  that  it  nearly  always  cokes  well 
whenever  attaining  anything  like  its  normal  thickness  and  hence  in 
several  regions  is  locally  known  as  the  “coking  veiu.’7  There  are  many 
districts  where  this  bed  will  produce  coke  but  little  if  any  inferior  to 
that  of  the  Pittsburgh,  in  the  famous  Connellsville  basin,  and  when  the 
latter  is  exhausted  the  next  source  of  supply  to  the  Pittsburgh  and 
Pennsylvania  region  generally  must  come  largely  from  this  horizon. 
Still  another  feature  of  this  coal  is  its  tenderness,  and  by  this  it  can 
often  be  distinguished  from  the  very  hard  Mahoning  coal  next  above 
(which  often  rivals  this  bed  in  size),  since  as  a rule  the  coal  from  the 
Upper  Freeport  horizon  does  not  bear  much  handling  without  breaking 
up  most  of  the  lumps,  although  they  often  come  out  of  the  mine  with 
large  size.  This  is  true  of  the  bed  everywhere  in  Pennsylvania  and 
West  Virginia  (except  in  the  southwestern  part  of  the  latter  State,  where 
it  is  often  a splint  coal),  and  Prof.  Orton  reports  the  same  thing  as  char- 
acterizing it  all  over  the  Ohio  field. 

There  is  frequently  a layer  of  impure  cannel  or  highly  bituminous  slate 
in  the  roof  of  this  coal,  and  in  the  Great  Kanawha  region  a fine  deposit 
of  cannel  coal  occurs  at  this  horizon.  This  is  true  of  the  Cannelton 
locality,  but  whether  any  of  the  cannel  deposits  on  Coal  River,  south 
from  the  Kanawha,  belong  at  this  same  geological  level  is  as  yet  unde- 
termined, since  the  latter  have  not  been  sufficiently  studied,  though  the 
flora  would  indicate  that  the  Peytona  deposit  belongs  at  the  horizon 
of  the  Upper  Kittanning  coal. 

The  several  sections  that  have  already  been  given  (Kos.  50-121),  in- 
dicate the  structure  of  the  Upper  Freeport  bed  in  many  regions,  but 
there  remain  others  where  it  is  equally  important,  and  some  of  these 
will  now  be  given. 

Section  at  McCoy  shaft,  near  Oallitzin,  Cambria  County,  Pennsylvania. — 
Some  large  coke  plants  have  recently  been  put  into  operation  on  this, 
bed  along  the  line  of  the  Pennsylvania  Railroad  and  its  branches  on 
the  summit  of  the  Alleghany  Mountains  in  Cambria  and  Clearfield 


WHITE.]  THE  UPPER  FREEPORT  COAL.  149 

Counties.  At  the  McCoy  shaft,  near  Gallitzin,  the  coal  has  the  follow- 
ing structure,  according  to  the  superintendent’s  statement: 

• Ft.  in. 


Black  slate  and  bone  coal 0 8 1 

Slate,  gray 0 2 I Ft-  in* 

Coal 1 0 > 6 5 

Slate  0 3 | 

Coal 0 4 J 


Section  near  eastern  end  of  old  Portage  Railroad  tunnel , at  Gallitzin , 
Pennsylvania. — Near  the  eastern  end  of  the  old  Portage  Railroad  tun- 
nel, at  Gallitzin,  the  coal  is  well  exposed,  and  there  shows  as  follows  : 


Coal 

Dark  slate  and  bony  coal 

Coal 

Slate,  gray  

Coal 

Slate  and  slaty  coal 


Ft.  in. 

0 4 ^ 

0 2 j 

3 0 I Ft*  in- 

0 2 

1 2 
0 10  J 


> 5 8 


According  to  Messrs.  Chance  and  Platt,  this  coal  is  but  poorly  repre- 
sented in  the  present  mining  regi<  ns  of  Clearfield  and  Jefferson  Coun- 
ties, Pennsylvania,  but  it  is  possible,  as  already  suggested  in  connec- 
tion with  section  88,  that  in  some  cases,  at  least,  the  Upper  Freeport 
coal  may  have  been  erroneously  referred  to  the  horizon  of  the  Lower 
Freeport. 

Section  at  Mount  Equity  mine , Bedford  County , Pennsylvania . — In  the 
Broad  Top  field  this  coal  is  finely  developed  in  Bedford  County,  where 
it  is  known  as  the  “ Kelly  seam,”  and  exhibits  the  following  structure  at 
the  Mt.  Equity  mine,  according  to  Stevenson,  Report  T2,  Second  Geo- 
logical Survey  of  Pennsylvania,  page  62 : 

Ft.  in. 


Coal 2 1 

Parting 

Coal 0 7 

Parting Ft.  in. 

Coal 1 2 7 2 

Parting 

Coal 1 0 

Clay 2 0 

Coal 0 4 . 


Although  this  bed  is  so  well  developed  in  Bedford  County,  yet  when 
followed  northward  into  Huntingdon,  only  10  miles  distant,  it  thins 
away  to  only  1 foot  or  even  less. 

Followed  southward  from  Cambria  County  along  the  Alleghanies, 
this  coal  becomes  quite  thin  and  slaty  in  Somerset,  and  where  the  bed 
enters  Maryland  near  the  northern  end  of  the  Georges  Creek  basin,  it 
is  only  8 to  4 feet  thick  and  quite  slaty,  there  being  a layer  of  bony, 
worthless  coal,  1 foot  thick,  just  above  the  middle. 


150 


THE  NORTHERN  BITUMINOUS  COAL  FIELD. 


(BULL.  65. 


This  poor  condition  of  the  bed  seems  to  be  maintained  southward 
along  the  Georges  Creek  basin  to  Piedmont  (Section  92)  and  up  the 
North  Potomac  (Section  93)  to  near  its  source  (Section  94)  before  the 
coal  becomes  valuable  again,  since  there  the  whole  bed  thickens  up  to 
8 feet,  and  is  extensively  mined  at  Thomas,  on  the  West  Virginia  Cen- 
tral Railroad,  in  spite  of  the  fact  that  2 feet  of  bony,  worthless  coal  still 
remains  near  the  center  of  the  bed. 

In  the  Ligonier  basin  of  Westmoreland  and  Fayette  Counties,  Penn- 
sylvania,  Prof.  Stevenson  reports  this  bed  of  inferior  quality,  being 
filled  with  knife  edges  of  slate  and  containing  too  much  sulphur  for  the 
manufacture  of  coke,  though  it  often  has  a good  thickness.  This  con- 
dition of  affairs  is  continued  southward  along  the  Ligonier  basin  into 
Preston  County,  West  Virginia,  until  we  begin  to  approach  the  vicin- 
ity of  Cheat  River,  when  a great  change  takes  place  in  the  character 
of  the  coal,  the  sulphur  and  thin  slates  disappearing  and  the  whole  be- 
coming a most  valuable  coking  coal. 

Section  at  Posters  bank , near  Masontown , Preston  County , West  Vir- 
ginia.— The  section  at  Mr.  Posten’s  bank,  2 miles  from  Masontown, 
Preston  County,  shows  the  following  structure : 

Ft.  in. 

Coal,  slaty 1 3 ^ 

Coal,  good 3 0 I 

Slate,  gray 0 3 ! ^ m* 

Coal,  good 1 3 > y 7 

Shale 0 10  | 

Coal,  good 3 0 j 


This  is  near  the  center  of  the  basin,  and  the  coal  is  there  thicker 
than  the  average. 

Section  at  Hartleys  bank , near  Masontown , Preston  County , West  Vir- 
ginia.— The  following  from  the  side  of  the  trough  near  Masontown,  at 
Mr.  Hartley’s  bank,  will  better  represent  the  average  thickness  of  this 
coal  in  the  Preston  basin : 


Slaty  coal.. 
Coal,  good.. 
Shale,  gray 
Coal,  good.. 
Shale,  gray 
Coal,  good. 


Ft.  in. 


0 2 I Ft-  in- 

1 3 > 8 7 

1 0 

1 6 , 


The  first  parting  below  the  top  is  usually  called  the  “little”  slate, 
while  the  next  one  is  known  as  the  “ big  ” slate. 

This  is  the  same  coal  that  has  long  been  coked  for  the  manufacture 
of  iron  at  Irondale,  Preston  County,  and  also  near  Austin,  on  the  Balti- 
more and  Ohio  Railroad.  At  both  of  these  localities  the  coal  below 
the  “ big  ” slate  is  not  taken  out  on  account  of  the  expense  of  mining 
the  latter. 

Southward  from  the  Baltimore  and  Ohio  Railroad  this  bed  again 
splits  up  with  numerous  slate  partings,  and  when  it  comes  out  to  day- 


WHITS.] 


THE  UPPER  FREEPORT  COAL. 


151 


light,  on  the  Valley  River,  at  Philippi,  the  coal  is  4 feet  thick,  but  so 
slaty  as  to  be  almost  valueless,  and  only  20  to  25  feet  above  the  Lower 
Freeport  coal. 

Section  at  Wilson's  mine , Roaring  Greek , Randolph  County , West  Vir- 
ginia.— South  ward  from  Philippi  it  increases  in  thickness,  and  when  we 
come  to  the  eastern  side  of  the  Belington  basin  the  bed  has  a total 
height  of  10  to  15  feet,  and  is  locally  known  as  the  Roaring  Creek  vein. 
Its  structure  there  is  shown  by  the  following  section  at  Mr.  William 
Wilson’s  mine,  in  the  northern  edge  of  Randolph  County,  and  about  1 
mile  east  from  the  Valley  River,  at  the  mouth  of  Roaring  Creek : 


Coal,  slaty,  impure  ... 

Shales,  dark 

Coal,  “ upper  bench  ” 
Slate  and  bony  coal... 

Coal,  “breast” 

Slate,  gray 

Coal,  “mining  ply”  . 

Clay  and  slate 

Coal,  “ bottom,”  slaty 


Ft.  in. 

1 6 
2 0 
2 8 
1 3 

3 i y 
0 6 
1 8 

0 4 

1 0 j 


Feet. 

14 


At  some  localities  the  u bottom  ” and  u mining  ply  ” benches  form  one 
layer  of  coal  3 to  4 feet  thick,  but  as  a rule  the  “ bottom  ” portion  is 
slaty  and  worthless,  while  the  u mining  ply”  and  the  u breast”  layers 
furnish  very  good  fuel,  the  “ upper  bench”  being  frequently  slaty  and 
otherwise  impure. 

Followed  still  farther  southward  along  the  eastern  side  of  the 
Appalachian  field,  through  Randolph,  Upshur,  Lewis,  Webster,  Nich- 
olas, Fayette,  Kanawha,  Lincoln,  Cabell,  and  Wayne  Counties,  West 
Virginia,  this  coal  bed  presents  the  features  shown  in  the  sections  given 

below. 


Section  on  Stone  Goal  Run , TJpshur  County , West  Virginia. — In  Upshur 
County,  10  miles  west  from  the  Roaring  Creek  region,  the  Upper  Free- 
port coal  is  exposed  on  Stone  Coal  Run,  a tributary  of  the  Big  Sandy, 
which  empties  into  the  Buckhannon  River.  Here  the  following  struct- 
ure is  visible : 

Ft.  in. 


Black  slate 

Coal 

Bony  coal  . . 

Coal 

Black  slate 

Coal 

Gray  slate. 

Coal 

•Slate,  dark 

Coal 

Slate,  dark 
Coal,  slaty. 
Slate,  gray 
Coal 


6 

0 

8 

0 

0 

0 

6 

r> 

4 

10 

5 

5 

6 


Ft.  in. 
14 


i 0 

V,  rO 

f a 


Ft. 
> 22 


7 4 


152  THE  NORTHERN  BITUMINOUS  COAL  FIELD.  [bum,.  65. 

This  is  the  locality  of  the  celebrated  u 22-foot”  coal  bed  of  Upshur 
County.  The  detailed  structure  above  given  does,  indeed,  exhibit  a 
bed  of  this  enormous  thickness,  but  it  is  so  split  up  with  slate  as  to  be 
practically  worthless. 

Section  on  the  Buckhannon  River , Up  liur  County . West  Virginia. — Still 
further  west  from  this,  on  the  main  Buckhannon  Biver,  one-fourth  of  a 
mile  above  Grassy  Run  and  9J  miles  from  Buckhannon  town,  in  a cut 
on  the  West  Virginia  and  Pittsburgh  Railroad,  the  following  section  is 
exhibited : 


Massive  sandstone  (Lower  Mahoning) 

Feet. 

f Cannel  slate 

12' 

0"1 

1 Coal 

2' 

0"  1 

Upper  Freeport  coal..  <(  , 

| Shale 

2' 

0"  [ 

....  17 

f Coal 

V 

0"J 

Gray  shale 

....  3 

Concealed 

....  10 

Massive  sandstone  in  bed  of  Buckhannon  River 

....  5 

Here  the  coal  has  almost  entirely  disappeared  in  the  great  mass  of 
cannel  slate  at  the  top,  which,  of  course,  contains  a large  quantity  of 
bituminous  matter. 

Section  at  Lloyd  Wamsley’s  bank.  Upshur  County , West  Virginia. — About 
10  miles  south  from  the  last  locality  we  come  to  an  area  of  this  coal  be- 
tween the  main  Buckhannon  River  and  its  middle  fork,  where  it  has 
regained  a structure  more  nearly  normal,  viz: 


Ft.  in. 

Cannel  slate 0 7 

Coal 2 7 

Slate,  black 0 4 

Coal 0 8 

Shale,  gray 0 8 

Coal,  soft ..  1 7 


Mr.  Bryan's  bank , one  half  mile  northwest,  exhibits  the  following: 


Ft.  in. 


Cannel  slate 0 6 

Coal 2 0 

Bony  coal 0 6 

Coai 3 0 


Section  at  Current’s  farm , Upshur  County,  West  Virginia. — A few  miles 
so  uth  of  this,  near  the  Randolph  County  line  this  coal  passes  into  the 
air  on  the  land  of  Mr.  Current,  where  it  exhioits  the  following: 


Sandstone . . . 

Coal 

Slate,  blue  .. 

Coai 

Clay 

Coal 

Sand  rock  ... 
Coal,  visible 


Ft.  in. 

1 oi 

2 2 I 
0 2 ! 
0 10  * 

0 G 

1 0 
1 0 


Ft.  in. 
25 

6 8 


WHITE.] 


THE  UPPER  FREEPORT  COAL. 


153 


Section  near  Hacker's  Valley  P.  0.,  Webster  County , West  Virginia. — 
Southward  from  this,  through  the  edge  of  Randolph,  the  coal  has  been 
eroded  by  the  waters  of  the  Buckhannon,  but  beyond  Helvetia  and  the 
Florence  Pass  we  come  to  an  elevated  plateau,  from  which  the  Buck- 
hanuon,  Little  Kanawha,  and  Holly  (a  tributary  of  the  Elk)  Rivers  all 
take  their  rise,  and  here,  in  Webster  County,  7 miles  northeast  from 
Hacker’s  Valley  post-office,  we  catch  an  outlier  of  this  coal  with  the 
following  structure: 

Ft.  in. 

Coal,  good 1 3 ! Ft- in* 

Bony  coal 1 2 j ^ ^ 

Coal,  good 2 8 J 


Section  on  the  Little  Kanawha  River , Lewis  County , West  Virginia. — 
About  10  miles  northwest  from  this  last  locality  the  same  coal  exhibits 
the  following  structure  (according  to  William  S Stevenson)  in  the  hills 
along  the  Little  Kanawha  River,  where  the  left  branch  of  that  stream 
cuts  across  the  panhandle  of  Lewis  County: 

Ft.  in. 

Slaty  coal 5 O') 

Coal,  hard - 2 8 

Slate 0 8 j 9 0 

Coal,  softer 1 8 J 


Section  on  the  'Holly  River , Webster  County , West  Virginia. — In  the 
summit  of  the  hills  near  Anderson’s  mill,  on  the  left  branch  of  Holly 
Liver,  Webster  County,  we  find  the  Upper  Freeport  coal  with  the  follow- 
ing structure  on  the  land  of  Mr.  Marcum  Cougar: 


Coal,  hard 
Slate,  dark 
Coal,  soft. 
Bony  coal 
Coal,  soft. 


Ft.  in 
3 2 

0 4 

1 4 

0 4 

1 8 


Ft.  in. 
6 10 


Section  at  Powell  Mountain , Nicholas  County , West  Virginia. — To  the 
southwest  from  this  there  are  no  more  openings  on  this  coal  until  we 
come  to  Powell  Mountain,  in  Nicholas  County,  although  a u 7-foot” 
bed  of  coal  is  frequently  “reported”  in  the  hills  where  the  Upper  Free- 
port ought  to  be  found.  But  in  Powell  Mountain  it  has  been  mined 
for  a long  time  on  the  Weston  and  Gauley  Bridge  turnpike,  where  it 
exhibits  the  following  structure: 

Ft.  in. 

Coal,  blossom ') 

Shales,  gray 10  0 j Ft.  in. 

Coal,  splinty 2 0 ) 14  3 

Black  slate • 0 3 | 

Coal,  splinty  2 0 J 


Here  the  character  of  the  coal  begins  to  change  to  the  hard,  splinty 
variety  which  distinguishes  the  coals  of  tiie  Kanawha  Valley. 


154 


THE  NORTHERN  BITUMINOUS  COAL  FIELD. 


[BULL.  65. 


Section  on  Stroud  Creel',  Nicholas  County , West  Virginia. — A few  miles 
east  from  this,  on  the  waters  of  Stroud  Creek,  this  bed  shows  the  follow- 
ing section  on  the  land  of  Dr.  D.  M.  Lewis : 


Carmel 

Coal,  splint 

Soft  coal 

Black  slate 

Coal 

Black,  coaly  slate 

Gray  slate 

Coal,  soft 

Clay 

Coal,  soft 

Slate  

Coal 


Ft. 

in. 

0 

51 

. 4 

° 

. 0 

4 

. 0 

1 

. 0 

6 

. 0 

6 ) 

. 3 

0 

. 1 

10 

. 1 

0 

. 0 10 

. 0 

1 

. 0 

3 J 

Sections  on  Mumble  the  peg  Creek , Nicholas  County , West  Virginia. — On 
Mumble-the-peg  Creek,  half  way  between  Powell  Mountain  and  Nicho- 
las Court-House,  we  find  an  opening  in  the  Upper  Freeport  coal  on 
the  land  of  Mr.  Herold,  where  it  shows  the  following  structure: 


Coal 

Shales 

Cannel 

Coal,  splinty, 
Slate,  black  . 
Coal,  splinty 


Ft.  in. 


1 61 
5 0 ‘ 
0 8 
2 ' 6 
1 8 
2 6 


Ft.  in. 
13  10 


At  another  bank,  300  yards  west  from  the  last,  the  following  is  seen: 


Ft.  in. 


Coal,  blossom 
Shale,  gray.. 
Bony  cannel . . 
Coal,  splinty 
Slate,  black  . 
Coal,  splinty 


1 

2 0 I 
0 6 l 
2 1 ( 
0 3 I 

2 6 j 


Ft.  in. 
7 4 


At  this  locality,  as  well  as  iu  Powell  Mountain  and  on  Stroud  Creek, 
a very  good  quality  of  splint  coal  is  obtained  from  this  bed. 


From  Nicholas  Court-House  on  southwestward  to  the  Great  Kanawha 
Biver  no  openings  have  been  examined  along  the  crop  of  this  coal,  but 
at  Cannelton,  in  Fayette  County,  wre  find  it  a valuable  bed  of  cannel 
coal  with  a thickness  of  1£  to  4 feet,  while  2 to  2J  feet  of  bituminous 
coal  rests  immediately  on  the  latter. 

Two  miles  below  Cannelton,  at  the  mouth  of  Upper  Creek,  the  bed 
thickens  to  11  feet,  but  the  layers  of  coa)  are  so  interstratified  and 
diluted  with  slate  and  muddy  sediment  that  the  whole  is  worthless.  A 
few  miles  farther  down  the  Kanawha,  at  East  Bank  and  Crown  Hill,  a 
portion  of  this  great  bed  becomes  the  excellent  splint  coal,  3 to  4 feet 


thick,  which  is  mined  at  those  localities,  but  farther  down  this  river 
the  bed  again  becomes  impure  and  remains  practically  worthless  from 
Coal  burg  on  down  until  it  disappears  under  the  river  at  Charleston. 


WHITE.] 


THE  UPPER  FREEFORT  COAL. 


155 


West  from  the  Kanawha  we  have  no  information  about  this  coal  until 
we  reach  the  Guyandotte  River  in  Cabell  and  Lincoln  Counties,  but  it 
is  possible  that  some  of  the  Coal  River  cannel  belongs  at  this  horizon.' 

Section  on  the  Guyandotte  River , Cabell  County , West  Virginia . — On  the 
Guyandotte  River  the  Upper  Freeport  coal  rises  above  water  level  about 
two  miles  above  the  u Falls  Dam.”  It  is  first  opened  and  mined  at  the 
mouth  of  Stone  Coal  Run,  where  it  exhibits  the  following  structure : 


Coal 

Slate  

Coal 

Slate  and  bony  cannel 
Coal,  visible 


Ft  in. 

0 4 " 

0 2 Ft. 

0 7 } 3 

0 9 

1 8 J 


in. 

6 


Another  opening  a short  distance  up  the  run  gives  the  following: 


Massive  sandstone 

Cannel  slate 

Slate 

Coal,  good 


Ft.  in.  Ft.  in. 

25  0 

1 °1 

0 3 > 5 3 

4 0 j 


This  latter  section  very  probably  belongs  immediately  on  top  of  the 
first  opening,  since  the  interval  between  the  two  banks  is  concealed. 

The  coal  is  known  in  this  region  as  the  u big  bed.”  On  the  Caldwell 
tract,  opposite  Camp  Branch,  this  coal  exhibits  the  following  section  in 
the  bluff  overlooking  the  Guyandotte: 


Sandstone,  visible 


Ft.  in. 
10  0 


Coal, 


Upper  Freeport.. 


'Coal,  slaty.. 

...  V 

0"1 

Coal 

....  V 

6" 

Slate  

....  07 

1" 

Coal 

....  2' 

0" 

Slate  

....  O' 

2"  l 

j Coal 

....  O' 

9"  i 

! Shale 

...  O' 

9" 

Coal 

....  0' 

8" 

Slate  

....  0' 

6"  I 

tCoal 

0"j 

10  5 


As  will  be  perceived,  the  coal  contains  much  slaty  material  and  the 
layers  of  coal  themselves  are  inclined  to  be  bony  and  impure,  approach- 
ing the  type  which  this  bed  exhibits  in  the  vicinity  of  the  Kanawha 
Mining  Company’s  plant  on  the  Big  Kanawha  River. 

Sections  on  Cove  Creelc.  Wayne  County , WestVirginia. — As  we  pass  from 
the  Guyandotte  in  Lincoln  County  westward  across  the  divide  to  the 
waters  of  Twelve  Pole,  a great  change  takes  place  in  the  Upper  Free- 
port bed,  and  on  Cove  Creek  we  find  it  split  into  two  portions  with  30 
feet  of  rock  between,  and  the  lower  bench  a fine  quality  of  cannel  coal 
3 to  4 feet  thick  at  some  openings. 


THE  NORTHERN  BITUMINOUS  COAL  FIELD. 


156 


[BULL.  C.p 


At  another  locality  the  following  is  seen  : 

Ft.  in. 

Coal  blossom 2 O') 

Shales  and  sandstone 30  0 j 

Shale O'  6,/'j  > 

Coal,  splint 1'  8"  ! j 

Cannel,  good V 4"  f *"  4 1U  J 

Coal,  bony 1'  4 " j 


m. 

10 


On  the  opposite  side  of  Cove  Creek  we  see: 


Ft.  in. 

Massive  sandstone 

Coal 0 6 

Slate 0 4 [ rt-  in* 

Coal 1 6 f 5 4 

Cannel 3 0 j 


From  this  point  a belt  of  cannel  coal  at  the  horizon  of  this  bed  ex- 
tends in  a general  westerly  direction  nearly  across  Wayne  County,  being 
found  on  all  ot  the  main  branches  of  Twelve  Pole.  It  is  possibly  identi- 
cal with  the  celebrated  Moses  Fork  cannel  and  other  cannel  deposits 
in  Kentucky.  This  belt  of  cannel  varies  much  in  width,  but  it  is  often 
2 or  3 miles  across,  and  while  the  bed  is  not  entirely  persistent,  it  is 
seldom  less  than  20  inches  thick.  It  is  quite  pure  and  will  compare 
favorably  with  the  celebrated  Kanawha  cannel,  which  comes  at  the  same 
geological  horizon. 

On  the  left  branch  of  Twelve  Pole , one-half  mile  above  the  mouth  of 
Brush  Creek,  this  cannel  coal  shows  as  follows  : 

Ft.  in. 

Massive  sandstone - 

Coal,  bituminous 0 10")  ^ 

Rock,  dark 0 8 4 

Cannel 2 6 j 


On  Little  Laurel , a branch  of  Hezekiah  Creek  (tributary  of  the  left 
fork  of  Twelve  Pole),  the  cannel  exhibits  the  following: 

Ft.  in. 

Sandstone 

Coal,  bituminous 1 O') 

Bone  coal 0 8 I in* 

Cannel 3 If 

Bone  coal * 1 8j 


WHITE.] 


THE  UPPER  FREEPORT  COAL. 


157 


0 
6 

1 
3 

7 
0 
5 
5 
2 

8 

5 

6 J 


Feet. 

27 


On  /Saw  Pit  branch  of  Cove  Creek  the  following  section  was  meas- 
ured : 

Ft.  in. 

Coal,  blossom 2 0 ) 

Sandstone  ■- 25  0 S 

Coal 0 

Slate,  gray 0 

Coal,  bituminous 1 

Cannel 1 

Coal,  splint  1 

Slate  and  slaty  coal 0 

Coal  0 

Slate 0 

Coal,  splint 0 

Slate,  blue 0 

Coal,  splint 1 


8 


In  Sugar  Camp  Hollow , a short  distance  above  Jesse  Queen’s,  the 
Upper  Freeport  coal  exhibits  the  following  structure: 

Ft.  in. 

Sandstone,  massive ^ 

Coal 2 4 

Slate 0 2 

Coal,  splint « 1 2 

Slate,  gray 0 4 

Coal r 0 2 

Slate,  gray 0 4 


Coal,  splint 0 8 f 

Slate,  gray 0 4 

Coal 1 6 

Slate,  dark 0 9 

Coal  0 7 

Slate 0 6 

Coal 0 1 J 

Shaly  sandstone 15 

Coal 1 


Ft.  in. 

8 11  1 


Ft.  in. 
25  5 


6 J 


On  Trough  Creelc , near  James  Rainey’s,  this  coal  exhibits  the  fol- 
lowing: 


Massive  sandstone 

Ft. 

in. 

Cannel  slate 

....  0 

5 

Coal,  splinty 

9 

Slate  

0 

1 

Coal,  splint 

1 

0 „ 

Flaggv  sandstone  and  shale 

Cannel  slate 

0 

8 ' 

Coal 

p. 

1 

Slate  

0 

a 

Coal 

....  0 10  [ 

Shale,  gray 

6 1 

Coal 

lj 

Ft.  in. 

3 S') 


Ft.  in. 
24  7 


158 


THE  NORTHERN  BITUMINOUS  COAL  FIELD. 


[bull.  65. 


At  Greene  Porter’s,  on  tlie  right  bank  of  Twelve  Pole,  the  Upper 
Freeport  bed  shows  the  following: 


Ft.  in. 


Coal 


. Clay 

Shale  and  coal 

Coal 

Bony  coal  and  slate 
Coal 


1 0 4 
0 5 

0 9 

1 10  | 

1 0 j 

2 4 j 


Ft.  in. 
7 4 


From  this  point  on  west  to  the  Kentucky  line  on  the  Tug  River  noth- 
ing is  known  of  the  Upper  Freeport  coal,  and  at  Warfield  it  seems  to 
be  absent  from  the  section,  but  this  may  possibly  be  due  to  the  fact 
that  its  horizon  there  overtops  the  summit  of  the  hills. 

In  western  Pennsylvania  there  are  large  areas,  especially  in  Beaver 
County,  where  this  coal  is  either  absent  or  else  too  thin  to  mine ; so  it 
enters  Ohio  not  as  a persistent  bed,  but  occurring  in  patches,  and  this 
characteristic  seems  to  remain  with  it  there,  from  the  Pennsylvania  line 
entirely  across  the  State  to  the  Kentucky  border  at  Ironton. 

Even  along  the  Ohio  River  from  the  Pennsylvania  line  down  to  where 
this  bed  dips  below  the  same,  it  is  generally  absent,  and  Prof.  Orton 
thinks  it  is  still  absent  in  the  Steubenville  shafts,  the  coal  mined  there 
being  the  Lower  Freeport  bed,  instead  of  the  Upper  Freeport  as  was 
formerly  supposed. 

In  eastern  Ohio  it  is  known  as  bed  No.  6 in  the  Ohio  scheme  of  num- 
bers, but  in  other  portions  of  the  State,  as  Prof.  Orton  has  shown,  it 
was  often  called  No.  7.  The  following  list  of  Ohio  names  for  this  bed 
will  indicate  regions  in  that  State  where  the  bed  becomes  prominent: 
“Big  Vein”  of  Salinesville,  “Dell  Roy,”  “Cambridge,”  “Alexander,” 
“Bayley’s  Run,”  “ Norris,”  “ Happy  Hollow,”  “Waterloo.” 

Section  near  Kenova , West  Virginia. — After  passing  beneath  the  Ohio 
River  above  Steubenville,  this  bed  never  emerges  from  the  same  until 
within  2 miles  of  the  Kentucky  line,  and  if  the  Steubenville  shaft 
coal  be  the  Lower  Freeport,  then  the  Upper  one  is  absent  over  a wide 
region  along  the  Ohio  River,  for  it  appears  to  be  absent  in  several  bor- 
ings, notably  at  Parkersburg  and  Pomeroy.  It  is  reported  from  a boring 
at  Huntington,  however,  as  10  feet  thick,  though  where  it  comes  up  to 
the  level  of  the  Chesapeake  and  Ohio  Railroad  at  the  east  end  of  the 
Big  Sandy  bridge,  10  miles  below  Huntington,  the  bed  is  worthless, 
as  shown  by  the  following  structure  there : 

Ft. 

l 1 Ft. 

3 J,  5 

1 j 


Coal 

Shale 

Coal,  slaty 


WHITE.  J 


THE  UPPER  FREEPORT  COAL. 


159 


Section  in  RitcMe  County , West  Virginia. — Where  this  bed  is  brought 
to  the  surface  on  the  Volcano  anticlinal  in  Ritchie  County,  West  Vir- 
ginia, it  has  the  following  structure,  according  to  Stevenson : 

Ft.  in. 

Coal 2 6 ^ Ft.  in. 

Sandstone,  gray r..  3 6 6 8 

Coal 0 8 J 

THE  UPPER  FREEPORT  LIMESTONE. 

Below  the  coal  just  described,  at  an  interval  which  varies  from  0 to 
40  feet,  there  comes  a limestone  which  was  named  from  the  same  local- 
ity as  the  coal.  It  is  quite  generally  distributed  in  Pennsylvania,  north- 
ern West  Virginia  and  Ohio,  but  in  the  southwestern  part  of  West 
Virginia  it  appears  to  be  absent,  since  it  has  never  been  reported  from 
the  region  along  the  Big  Kanawha  and  its  tributaries,  nor  from  the 
region  between  that  and  the  Big  Sandy.  • 

The  limestone  is  usually  of  a light  gray  color  on  fresh  fracture,  but 
some  of  the  layers  are  always  buffish  when  weathered,  owing  to  in- 
cluded iron.  Frequently  the  rock  presents  a brecciated  aspect,  as  if 
made  from  the  broken  fragments  of  an  older  limestone. 

Fossils  are  rare  in  this  bed  except  a minute  univalve  which  looks  as 
if  it  might  be  of  fresh  water  origin.  Some  layers  of  this  stratum  gen- 
erally contain  a considerable  amount  of  carbonate  of  magnesia,  and 
occasionally  enough  to  constitute  it  a good  rock  for  the  manufacture  of 
hydraulic  cement. 

The  thickness  varies  from  1 foot  up  to  30  feet  as  a maximum,  though 
the  average  might  be  placed  at  5 to  8.  It  makes  an  excellent  lime  for 
fertilizing  purposes,  and  is  much  sought  after  to  enrich  the  barren  soil 
lauds  above,  though  it  is  occasionally  mined  for  use  in  blast  furnaces, 
as  on  the  Alleghany  River  between  Freeport  and  Kittanning,  where  it 
is  unusually  thick. 

In  Ohio  this  bed  has  been  given  several  names,  as  u Shawnee,” 
u White,”  u Buchtel,”  etc.  There,  also,  as  in  Pennsylvania  and  West 
Virginia,  it  occasionally  becomes  iron-bearing  and  some  or  all  of  its 
layers  develop  into  iron  ore,  which  is  known  in  Ohio  as  the  “Buchtel” 
ore,  and  in  Pennsylvania  as  the  “ Summit”  ore. 

THE  BOLIVAR  FIRE  CLAY. 

When  the  Upper  Freeport  limestone  is  absent,  or  but  slightly  rep- 
resented, there  occasionally  comes  into  the  section  at  its  horizon  a bed 
of  excellent  fire  clay,  which  from  having  long  been  mined  near  Bolivar, 
Westmoreland  County,  Pennsylvania,  is  generally  known  as  the  Bolivar 
clay.  As  there  developed  it  shows  a fine  quality  of  non-plastic  clay 
which  is  used  in  the  manufacture  of  fire  brick  and  gas  retorts.  Tt  also 
occurs  in  several  other  regions  of  Westmoreland  County,  as  well  as  in 
Fayette  and  other  Pennsylvania  counties. 


160 


THE  NORTHERN  BITUMINOUS  COAL  FIELD. 


[BULL.  65 


This  clay  has  been  reported  as  valuable  at  only  two  or  three  points 
in  Ohio,  viz,  in  Jefferson  and  Muskingum  Counties,  while  in  West  Vir- 
ginia it  is  known  to  be  valuable  in  only  one  region,  viz,  on  Deckers 
Creek,  in  Preston  and  Monongalia  Counties. 

THE  UPPER  FREEPORT  SANDSTONE. 

As  a rule  the  main  portion  of  the  interval  between  the  Upper  and 
Lower  Freeport  coals  is  occupied  by  sandy  shales  or  thin  flaggy  layers 
of  sandstone,  separated  by  shales,  but  occasionally  a bed  of  massive 
sandstone  makes  its  appearance  at  this  horizon  and  it  has  received  the 
name  of  Upper  Freeport  Sandstone.  It  is  quite  prominent  in  some  por- 
tions of  Pennsylvania,  but  appears  to  be  generally  absent  in  Ohio.  It 
is  also  conspicuous  along  the  Great  Kanawha  and  in  all  the  region  of 
West  Virginia,  southwest  from  there,  sometimes  attaining  a thickness 
of  75  feet,  while  in  Pennsylvania  it  is  seldom  more  than  30  feet. 

When  this  sandstone  is  not  present  as  a massive  rock  there  occasion- 
ally occurs  a thin  bed  of  coal  in  the  interval  between  the  Upper  and 
Lower  Freeport  coals,  and  I have  termed  it 

THE  MIDDLE  FREEPORT  COAL. 

This  bed  is  shown  in  Section  66  at  the  typical  Freeport  locality,  and 
as  already  stated  in  connection  therewith,  its  presence  in  other  sections 
may  have  led  to  some  confusion  in  identifications.  It  is  not  a regular 
member  of  the  series,  however,  and  is  probably  never  much  thicker  than 
at  Freeport,  viz,  2 feet. 

The  interval  between  the  Upper  and  Lower  Freeport  coals  varies 
greatly  in  thickness,  running  up  sometimes  to  80  and  again  thinning 
away  tq  20- odd  feet,  as  shown  in  Section  65. 

THE  LOWER  FREEPORT  COAL. 

This  bed  is  quite  as  variable,  or  even  more  so  than  the  Upper  Free- 
port above.  The  rule  is  that  whenever  one  of  these  beds  has  a fair 
development  the  other  is  poor  or  worthless,  but  in  addition  to  this  un- 
certainty, they  are  both  frequently  thin,  or  practically  absent  from  the 
section  at  the  same  time,  so  that  no  one  should  look  upon  any  of  these 
coal  beds  as  being  continuously  valuable  over  wide  areas. 

As  shown  in  Section  66  at  the  type  locality  of  this  bed,  it  is  even 
more  complex  in  its  structure  than  the  Upper  Freeport  above,  being 
split  into  two  well  defined  layers  separated  by  a stratum  of  clay  and 
limestone.  It  is  quite  probable  that  this  dividing  layer  may  at  times 
thicken  up  greatly  as  all  other  rocks  do,  and  separate  the  two  layers  of 
coal  by  an  interval  of  several  fret,  thus  making  two  apparently  distinct 
coal  beds,  but  which  should  really  be  classed  as  members  of  one. 

If  Messrs.  Chance  and  Platt  are  correct  in  the  identifications  of  the 
Lower  Freeport  coal  in  Jefferson  and  Clearfield,  there  are  large  areas 
in  both  of  these  counties  where  this  coal  is  quite  valuable,  since  it  is  4 


THE  LOWER  FREEPORT  COAL. 


WHITE.] 


161 


to  7 feet  thick  and  of  excellent  quality,  though  it  is  always  separated 
into  two  or  three  benches  by  partings  of  slate. 

The  upper  portion  of  the  Lower  Freeport  bed  often  has  a tendency 
to  become  cannelly,  as  at  Freeport,  and  some  highly  bituminous  shale 
is  frequently  present  at  this  horizon,  even  when  the  coal  is  absent. 

Another  very  fine  development  of  the  Lower  Freeport  coal  is  in  the 
vicinity  of  Fairmont,  Clarion  County,  Pennsylvania,  where  according  to 
Chance  it  is  5 to  7 feet  thick  without  any  partings,  and  furnishes  ao 
excellent  quality  of  gas  coal,  as  it  does  in  the  Reynoldsville  region  of 
Jefferson  County. 

In  Ohio  the  reputation  of  the  coal  as  a patchy  deposit  is  fully  sus- 
tained, since  Prof.  Orton  says  of  it  (Yol.  Y,  p.  16G,  Ohio  Geological 
Survey),  “this  is  a seam  the  horizon  of  which  can  be  followed  through- 
out the  entire  field,  but  which  becomes  workable  at  comparatively  few 
points.” 

In  eastern  Ohio  it  is  called  No.  5,  but  in  Stark  County  and  southwest- 
ward  it  is  known  as  No.  6a,  while  the  synonyms,  “ Whan”  ‘‘Steuben- 
ville Shaft,”  “Roger,”  “Hamden  Furnace,”  and  “Hatcher”  indicate 
localities  where  the  bed  becomes  important. 

If  the  “ Steubenville  Shaft”  bed  really  represents  this  coal  instead  of 
the  Upper  Freeport,  then  there  is  quite  a large  field  of  it  along  the  Ohio 
River,  for  it  is  found  of  good  thickness  in  every  boring  as  far  south  as 
Moundsville,  West  Yirginia,  where  it  underlies  the  Ohio  by  more  than 
600  feet. 

Section  near  Philippi , Barbour  County , West  Virginia. — In  Preston, 
Monongalia,  Mineral,  and  Tucker  Counties,  West  Yirginia,  this  bed  is 
quite  thin  and  often  absent  entirely,  so  it  is  not  mined  till- we  go  south 
into  Barbour  County,  where  it  thickens  up  and  in  the  vicinity  of  Phil- 
ippi exhibits  the  following  structure : 


Coal 

Slate  

Coal 

Slate  and  coal 
Coal 


Ft.  in. 

1 10  A 

0 8 Ft.  in. 

0 6 \ 5 10 

0 10  | 

2 0 J 


Nothing  is  known  of  the  Lower  Freeport  from  Philippi  on  southwest- 
ward  along  the  eastern  margin  of  the  Appalachian  field  until  the  Great 
Kanawha  River  is  reached,  except  in  the  Roaring  Creek  field,  where  it 
is  only  2 feet  thick  and  25  feet  below  the  upper  bed. 

But  from  the  fact  that  this  coal  becomes  one  of  the  principal  beds  in 
the  Kanawha  region,  and  from  there  on  southwestward  into  Kentucky, 
it  is  inferred  that  it  is  also  a valuable  bed  at  some  points  between  Phil- 
ippi and  the  Big  Kanawha. 

On  this  latter  stream  the  Lower  Freeport  appears  to  be  the  parent  of 
two  valuable  beds  known  respectively  as  the  Coalburg  and  Winnifrede 
veins.  The  former  certainly  belongs  to  this  horizon,  and  the  latter 

Bull.  65 U 


162 


THE  NORTHERN  BITUMINOUS  COAL  FIELD. 


f BULL.  65. 


probably  does,  though  formerly  I was  inclined  to  refer  it  to  the  horizon 
of  the  Upper  Kittanning.  The  Lower  Coal  Measures  thicken  up  so 
greatly  in  that  region,  however,  and  the  intervals  separating  the  Coal- 
burg  and  Winifrede  beds  from  the  top  of  the  series  and  from  each  other 
vary  so  much  that  it  seems  more  probable  they  are  both  members  of 
the  complex  Lower  Freeport  coal.  The  Coalburg  and  Winifrede  beds 
are  themselves  complex,  being  always  separated  into  two  or  three 
benches  by  layers  of  very  hard  slate  or  bony  coal  locally  known  as 
“nigger  head.’7  They  usually  furnish  the  variety  of  coal  known  as 
“splint,”  and  the  Kanawha  “splint”  is  highly  prized  as  a general  do- 
mestic fuel.  These  two  beds  are  quite  irregular  in  their  thickness  and 
one  or  both  are  often  too  thin  to  mine,  but  they  appear  to  be  much  more 
regular  and  persistent  southwest  from  the  Kanawha  than  the  Upper 
Freeport,  since  they  furnish  valuable  coal  clear  across  to  the  Big  Sandy 
Biver,  the  celebrated  Peach  Orchard  coal  of  Kentucky  coming  at  the 
horizon  of  either  the  Coalburg  or  Winifrede  bed,  or  both  combined. 
This  latter  view  is  the  more  probable,  since  at  the  tunnel  near  the  New 
Peach  Orchard  mine  the  coal  is  seen  splitting  up  till  it  is  scattered 
through  more  than  40  feet  of  rock  material. 

Section  of  bed  at  Coalburg , Kanawha  County , West  Virginia. — The 
following  section  shows  the  variations  in  the  structure  of  the  Coalburg 
bed  at  its  typical  locality : 


Splint  coal 

“Nigger  head” 

Splint  coal 

Shale 

Soft  coal 


6 in.  to  10  ft. 
4 in.  to  8 in. 
2\  ft.  to  3*  ft. 
1 ft.  to  8 ft. 
1 ft.  to  H ft. 


Section  at  Winifrede,  Kanawha  County , West  Virginia. — The  struc- 
ture of  the  Winifrede  coal  at  Winifrede  is  as  follows: 


Ft.  in. 

Gray  splint 0 5 

Soft  coal 0 5 

Gray  splint 0 3 

Soft  coal 0 3 

Gray  splint 1 2 

Soft  coal 1 3 

Slate 0 5 

Soft  coal 1 8 


| Ft.  in. 
I 4 10 


I do  not  know  of  any  locality  in  the  Kanawha  Yalley  where  both  the 
Winifrede  and  Coalburg  beds  are  mined  one  above  the  other  in  the 
same  hill,  for  when  one  is  good  the  other  happens  to  be  worthless,  and 
this  is  so  constantly  true  that,  were  it  not  for  the  fact  that  the  Coal- 
burg bed  is  only  100  feet  below  the  Kanawha  black  flint  while  the  Win- 
ifrede seam  is  175  to  200  feet  below  the  same  datum  line,  I would  be 
strongly  inclined  to  believe  that  they  were  one  and  the  same  coal. 

Section  at  mouth  of  Blaine  Creelc,  Lawrence  County , Kentucky. — In  de- 
scending the  Big  Saudy  Biver  the  Lower  Freeport  sinks  below  water 


VTOITB.] 


THE  LOWER  FREEPORT  LIMESTONE. 


163 


level  at  the  mouth  of  Blaine  Creek,  6 miles  below  Louisa,  where  it  ex- 
hibits the  following  structure : 

Ft.  in. 


Massive  sandstone  . 

Coal 

Fire  clay 

Sandy  shale 

Coal 

Shale  with  iron  ore 

Coal,  slaty 

Shale,  blue 

Coal 


. 0 10  | Ft- 
.5  0 > 7 

.2  0 j 
. 0 10) 

.1  0 [ 

. 1 0 }>  5 

1 q ! 


in. 

10 


7 


TILE  LOWER  FREEPORT  LIMESTONE. 


The  conditions  preceding  the  spread  of  a great  coal  marsh  seem  to 
have  been  eminently  fitted  for  the  production  of  limestone  deposits, 
especially  in  the  Pennsylvania  and  Ohio  regions,  for,  with  few  excep- 
tions, a limestone  is  found  close  under  every  coal  bed,  and  this  is  true 
of  the  Lower  Freeport  horizon.  This  limestone  very  much  resembles 
the  one  under  the  Upper  Freeport  coal,  except  that  it  is  usually  thinner 
and  more  earthy.  It  also  contains  the  same  univalve  fossil,  and  no 
others,  so  far  as  the  writer  is  aware,  thus  showing  that  it  too  is  a fresh- 
water deposit.  It  contains  a considerable  quantity  of  carbonate  of 
magnesia  and  occasionally,  as  at  the  locality  of  Section  103,  furnishes 
material  for  the  manufacture  of  hydraulic  cement. 

Considerable  iron  ore  is  also  found  at  this  horizon,  and  the  limestone 
is  generally  of  a buffish  cast  from  the  disseminated  iron.  From  this 
fact  it  and  the  Upper  Freeport  limestone  above  are  generally  called  the 
“buff”  limestones  in  southern  Ohio. 

In  West  Virginia  this  limestone  has  not  been  recognized  anywhere 
in  the  northern  part  of  the  State,  and  it  is  certainly  absent  entirely 
along  the  Great  Kanawha.  An  impure  limestone  is  sometimes  found 
in  connection  with  the  Peach  Orchard  coal  of  Kentucky,  which  is  pos- 
sibly identical  with  the  Lower  Freeport. 

THE  LOWER  FREEPORT  SANDSTONE. 

The  next  lower  stratum  that  has  a general  distribution  over  the  Appa- 
lachian field  is  known  as  the  Lower  Freeport  sandstone.  Section  66 
shows  the  thickness  and  structure  of  this  sandstone  at  its  typical 
locality,  and  there  it  is  seen  to  be  double,  with  a coal  embedded  in  its 
lower  portion,  the  whole  being  62  feet  thick.  That  the  15  feet  of  sand- 
stone under  the  coal  at  Freeport  belongs  properly  with  the  main  sand- 
stone above  is  known  from  the  fact  that  at  one  locality  the  coal  is  seen 
disappearing  entirely  and  then  the  two  beds  of  sandstone  unite  into 
one  solid  mass. 

This  rock  is  always  of  a grayish  white  color,  generally  quite  hard 
often  containing  pebbles  as  well  as  much  feldspar,  which  decomposing 
permits  the  rock  to  disintegrate  readily  and  weather  into  fantastic 


164 


THE  NORTHERN  BITUMINOUS  COAL  FIELD! 


[BULL.  65. 


shapes.  It  is  more  persistent  as  a massive  rock  than  the  Mahoning 
even,  but  unlike  the  latter  it  is  seldom  used  for  building  purposes. 
This  is  owing  to  its  hardness,  coupled  with  the  fact  that  it  will  not 
stand  the  weather  well,  and  also  it  is  often  so  gnarly  and  twisted  in  its 
bedding  that  it  will  not  split  evenly. 

This  sandstone  is  never  less  than  30  feet  thick  in  the  Pennsylvania 
region,  and  it  frequently  rises  to  75  and  even  100  feet  in  some  localities, 
making  a bold  cliff  or  bluff  wherever  its  outcrop  is  above  drainage,  and 
thus  becoming  a conspicuous  feature  in  the  topography  of  the  Lower 
Coal  Measures. 

Throughout  a large  portion  of  Beaver  County,  Pennsylvania,  this 
sandstone  is  75  to  80  feet  thick,  and  near  its  center  is  a very  hard 
calcareo- siliceous  layer  2 or  3 feet  thick,  which  may  possibly  represent 
the  Johnstown  Cement  limestone  in  other  portions  of  the  State. 

The  sandstone  maintains  about  the  same  thickness  throughout  east- 
ern Ohio  as  in  Beaver  County,  and  continues  on  around  to  southern 
Ohio  with  a thickness  of  30  to  50  feet. 

It  enters  West  Virginia  from  Pennsylvania  as  a very  massive  bed, 
50  to  75  feet  thick  in  Monongalia  and  Preston  Counties,  while  in 
Tucker,  Taylor,  Barbour,  and  Bandolph,  it  is  still  thicker  and  more 
pebbly  even  than  the  Pottsville  conglomerate.  South  westward  through 
Bandolph,  Webster,  Braxton,  and  Clay,  this  sandstone  keeps  on  increas- 
ing in  thickness,  and  when  the  Big  Kanawha  is  reached  it  has  swelled 
out  in  a wonderful  manner,  becoming  250  to  300  feet  thick,  and  remain- 
ing the  same  across  to  the  Big  Sandy,  often  crowning  the  hills  and 
ridges  with  cliffs  weathered  into  turreted  and  chimney-shaped  forms. 
When  attaining  this  immense  thickness  it  often  consists  of  three  or  four 
sandstones,  with  shales  and  two  or  three  coal  beds  in  ter  stratified. 

This  rock  has  produced  a small  quantity  of  oil  at  Fairview,  Marion 
County,  West  Virginia,  and  is  generally  known  as  the  “gas  sand,”  in 
the  drillers7  parlance,  since  it  often  produces  considerable  quantities  of 
natural  gas. 

THE  UPPER  KITTANNING  COAL. 

Throughout  several  counties  of  Pennsylvania  a third  bed  of  good 
coal  occurs  at  80  to  120  feet  below  the  top  of  the  series,  and  to  this 
Messrs.  Chance,  Platt,  and  other  Pennsylvania  geologists,  have  given 
the  name  Upper  Kittanning,  though  the  bed  in  question  is  not  work- 
able at  Kittanning  or  anywhere  near  that  town,  as  may  be  seen  from 
Sections  60-66  along  the  Alleghany  Biver,  since  it  is  thin  and  unim- 
portant in  that  region.  The  Messrs.  Platt  at  one  time  identified  this 
coal  with  the  Lower  Freeport  bed  in  Cambria,  Clearfield,  and  Jefferson 
Counties,  calling  the  coal  which  is  now  termed  Lower  Freeport  there 
the  Middle  Freeport,  and  it  is  barely  possible  that  this  first  arrange- 
ment of  the  stratigrapliical  order  was  the  correct  one  in  many  regions, 
since,  as  already  shown  (see  66),  there  is  a Middle  Freeport  coal  even 


WHITE.  J 


THE  UPPER  KITTANNING  COAL. 


165. 


at  Freeport,  and  in  addition  the  Lower  Freeport  bed  is  itself  so  com- 
plex that  either  half  of  it  might  at  any  time  separate  from  the  other 
and  both  become  independent  beds. 

But  however  the  questions  suggested  may  turn  out,  the  fact  remains 
that  at  many  localities  in  Pennsylvania,  at  least,  there  are  three  dis- 
tinct coal  beds  between  the  Ferriferous  limestone  and  the  Lower  Free- 
port coal,  as  shown  in  Sections  64,  65,  and  66. 

Westward  in  Ohio,  however,  the  Upper  Kittanning  coal  appears  to 
be  either  wanting  entirely  in  most  cases  or  else  coalesced  with  the 
Middle  Kittanning  bed,  since  Prof.  Orton  finds  no  place  for  it  as  a reg- 
ular member  of  the  Ohio  series,  but  puts  it  down  as  a synonym  for  the 
Lower  Freeport  seam.  (See  Yol.  V,  p.  126,  Ohio  Survey.) 

In  West  Virginia  the  Upper  Kittanuing  bed  first  appears  in  the  sec- 
tions along  the  Tygart’s  Valley  River  (96  and  97),  where  it  is  2 to  3J 
feet  thick,  and  a rather  fair  coal ; but  it  appears  to  be  absent  entirely 
in  the  Newburg  shaft,  Preston  County,  unless  it  is  combined  with  the 
Middle  Kittanning  there,  while  in  the  Korth  Potomac  basin  near  Davis 
it  is  represented  by  a mere  streak.  In  the  Kanawha  field  two  or  three 
thin  beds  come  at  this  horizon,  and  one  of  them  is  frequently  cannel, 
and  the  same  horizon  can  be  recognized  on  the  Guyandotte  River,  in 
Wyomiug  County  (Section  117). 

Chance  says  that  it  is  the  main  cannel  horizon  in  Pennsylvania,  the 
Kew  Bethlehem,  Korth  Washington,  and  Murrinsville  cannel  deposits 
coming  at  this  horizon.  If  the  Darlington  cannel,  of  Beaver  County, 
comes  at  this  same  horizon,  then  the  iuterval  separating  the  Upper 
and  Middle  Kittanning  beds  has  there  thinned  entirely  away,  and  thus 
brought  the  two  into  direct  contact.  This  might  well  be,  since  the  Dar- 
lington cannel  rests  directly  on  2 feefeof  bituminous  coal,  below  which, 
through  a shale  interval  of  30  feet,  comes  the  undoubted  Lower  Kit- 
tanning  coal,  underlaid  by  its  great  bed  of  fire  clay.  This  would  account 
for  the  absence  of  the  coal  in  Ohio,  if  it  really  does  unite  with  the  Mid- 
dle Kittanuing  before  crossing  the  Pennsylvania-Oliio  line. 

This  bed  appears  to  attain  its  greatest  importance  in  Pennsylvania, 
along  the  eastern  border  of  the  coal  field  through  the  counties  of  Jef- 
ferson, Clearfield,  Cambria,  and  Somerset,  where  it  has  been  fully  de- 
scribed by  Messrs.  Platt  and  Chance.  The  general  sections  already 
given  show  the  horizon  and  structure  of  this  bed  at  numerous  points, 
so  that  no  further  description  of  it  is  necessary. 

THE  JOHNSTOWN  (CEMENT)  LIMESTONE. 

Lying  only  2 to  5 feet  below  the  coal  just  described,  there  occurs,  Over 
a wide  region  in  Pennsylvania,  a bed  of  magnesian  limestone,  which  Mr. 
Franklin  Platt  named  the  Johnstown  Cement,  from  its  occurrence  at  the 
city  of  Johnstown,  Cambria  County.  It  is  almost  an  exact  counter- 
part of  the  Lower  Freeport  limestone  of  the  counties  farther  west  in 
physical  aspect,  chemical  composition,  fossils,  and  everything  else,  and 


166 


THE  NORTHERN  BITUMINOUS  COAL  FIELD. 


[BULL.  65. 


this  is  one  of  the  facts  which,  taken  in  connection  with  the  entire  ab- 
sence of  this  limestone  in  the  western  tier  of  counties  and  in  Ohio,  has 
sometimes  led  to  the  suspicion  that  possibly  the  Johnstown  Cement 
and  the  Lower  Freeport  limestone  of  Butler  and  Beaver  Counties  are 
identical.  Still  there  are  other  facts  of  stratigraphy  which  appear  to 
forbid  such  an  hypothesis,  and  hence,  until  it  can  be  shown  otherwise 
by  more  positive  demonstration,  we  must  accept  the  strati  graphical 
horizon  given  the  Johnstown  Cement  first  by  Messrs.  Platt,  whose 
labors  moved  it  up  from  the  horizon  of  the  Ferriferous  limestone,  to 
which  the  First  Geological  Survey  of  Pennsylvania  had  erroneously 
assigned  it.  The  stratum  ranges  in  thickness  from  1 to  8 feet,  and 
when  it  is  5 feet  or  more  some  of  the  layers  often  make  good  lime  for 
agricultural  or  other  purposes ; but  when  the  bed  is  only  1 to  3 feet 
thick  it  is  usually  too  impure  to  slake  well.  This  stratum  has  not  been 
recognized  at  any  point  within  West  Virginia  with  which  the  writer  is 
familiar,  and  it  thus  appears  to  be  generally  absent  from  the  series  in 
that  State. 

THE  MIDDLE  KITTANNING  COAL. 

Whatever  uncertainty  may  exist  concerning  the  exact  horizon  of  the 
coal  which  has  just  been  described  under  the  name  of  Upper  Kittan- 
ning, there  is  none  with  reference  to  the  next  lower  bed,  for  it  is  such 
a constant  member  of  the  series  that  its  relations  to  the  other  rocks  are 
seen  in  nearly  every  section.  This  bed  was  formerly  called  the  Upper 
Kittanning,  until  Messrs.  Platt  and  Chance  discovered  that  the  coal 
last  described  was  a member  of  the  Kittanning  group,  and  then  the 
coal  in  question  was  lowered  to  the  name  of  Middle  Kittanning. 

In  the  vicinity  of  Kittauning  (Section  63),  and  along  the  Alleghany 
Piver  below  (Sections  64,  65,  and  66),  this  bed  is  thin  and  unimportant, 
but  west  from  this  it  thickens  up  and  is  the  most  important  seam  in 
Butler,  Lawrence,  and  Beaver  Counties,  the  coal  being  quite  pure  and 
highly  esteemed  for  gas,  steam,  and  domestic  purposes,  though  it  sel- 
dom exceeds  4 feet  in  thickness,  and  is  often  much  less.  This  is  the 
famous  “ Clin  ton,”  “Rock  Point,”  and  “Hog  Hollow  ” coal  along  the 
Beaver  River.  It  is  always  divided  by  one  or  more  thin  slate  partings, 
one  of  which  is  usually  near  the  bottom. 

Eastward  from  Butler  County,  through  Armstrong,  Clarion,  Jeffer- 
son, and  Clearfield,  this  bed,  according  to  Platt  and  Chance,  declines 
much  in  thickness  and  value,  so  that  it  is  seldom  mined,  except  occa- 
sionally for  domestic  purposes. 

Still  farther  eastward,  however,  in  the  Broad  Top  coal  field  of  Hunt- 
ingdon and  Bedford  Counties,  it  thickens  up  and  is  apparently  repre- 
sented by  the  “Barnet”  coal  of  that  region. 

Southward  from  Pennsylvania,  in  Maryland  and  northern  West 
Virginia,  this  coal  is  sometimes  thick  enough  to  mine,  though  seldom 
exceeding  2J  to  3 feet.  At  the  southern  end  of  the  Korth  Potomac 


WHITE.] 


THE  MIDDLE  KITTANNING  COAL. 


167 


coal  basin  it  practically  unites  with  the  Lower  Kittanning  below,  and 
is  mined  with  the  latter  where  that  bed  is  opened  near  Thomas  ; but  at 
the  Davis  mine,  further  south,  the  parting  slates  have  thickened  up  to 
20  feet  and  separated  it  from  the  Lower  Kittanning  again. 

Section  at  Neioburg , Preston  County , West  Virginia. — In  the  deep 
shaft  at  Newburg,  Preston  County,  West  Virginia,  this  coal  has  the 
following  structure  and  relations  to  other  beds : 


1.  Lower  Freeport  sandstone 

Ft.  In. 

rCoal 1 oS 

o r.  I AT-  -Ml  tr-i  Slate 0 3 Ft.  in. 

2.  Coal,  Middle  Kit-  ^ Coal  dat  8 0 7 3 

tanninS | Clay 2 Ol 

fCoal,  good 2 0 j 

3.  Fireclay  and  stales - 15  0 

4.  Coal,  Lower  Kittanning,  with  several  partings 9 5 


Here  it  is  possible  that  both  the  Upper  and  Middle  Kittanning  beds 
are  represented  in  No.  2,  and  they  are  only  15  feet  above  the  Lower 
Kittanning  coal. 

In  the  Great  Kanawha  field,  this  bed,  although  only  3 to  4 feet  thick, 
is  very  pure  and  valuable,  being  known  there  under  the  names  of  “Ce- 
dar Grove,”  “Trimble,”  “Arno,”  and  others. 

In  the  Wyoming  County  section  (117)  two  beds  are  often  found  at 
this  horizon,  separated  by  20  feet  of  shales,  but  the  lower  one  appears 
to  be  the  main  coal.  The  same  thing  is  seen  in  the  Peach  Orchard 
section  (119),  where  the  lower  one  is  a “splint”  coal,  thin,  but  of  excel- 
lent quality. 

In  Ohio  this  coal  becomes  the  most  important  bed  of  all  the  coals  in 
that  State,  according  to  Prof.  Orton,  since  it  is  almost  constantly  work- 
able from  where  it  enters  Columbiana  County  on  the  east  to  where  it 
leaves  the  State  near  Ironton  at  the  southwest.  The  numerous  names 
it  has  received  in  Ohio  will  serve  to  illustrate  its  importance  in  the 
mining  industry  there,  of  which  the  following  is  a partial  list:  “ No.  4, 
in  Ohio  and  Yellow  Creek  Valleys  at  the  east;  “ No.  6,”  in  Stark  County 
and  southwestward;  “ Hammondsville  Strip  Vein,”  “ Onasburg,”  “ Pike 
Run,”  “Dennison,”  “Coshocton,”  “Upper  Zanesville,”  “Upper  New 
Lexington,”  “ Nelsonville,”  “ Straitsville,”  “Great  Vein”  of  the  Hock- 
ing Valley,  “ Carbondale,”  “Mineral  City,”  “Upper  Zaleski,”  “Wash- 
ington Furnace,”  “ Sheridan,”  etc. 

The  tracing  of  this  bed  through  Ohio,  and  its  identification  at  many 
points  where  it  had  formerly  been  confused  with  other  beds,  is  due 
largely  to  the  labors  of  Prof.  Orton,  the  present  efficient  director  of  the 
Ohio  Geological  Survey.  The  structure  of  the  coal  where  it  attains  a 
considerable  thickness,  as  in  the  Hocking  Valley,  is  always  quite  com- 
plex, there  being  several  parting  slates,  as  may  be  seen  from  Sections 
105  and  10G. 


168 


THE  NORTHERN  BITUMINOUS  COAL  FIELD. 


[BULL.  65. 


Section  in  Hoclcing  Valley,  Ohio. — The  following,  from  Yol.  Y,  Ohio 
Geology,  will  serve  to  illustrate  the  general  structure  of  this  bed  when 
at  its  maximum  development: 


Ft.  in. 

Top  coal ...2  7 ' 


Soft  coal,  rejected  0 4 

Coal 4 2 

Bone  coal,  rejected 0 6 [ 

Second  slate * 0 2 1 

Coal 1 6 

First  slate 0 1 

Coal 2 4 J 


Ft.  in. 
11  ? 


Section  at  Neic  Straitsville,  Perry  County. — The  following  is  the  struc- 
ture at  New  Straitsville,  p.  954,  loc.  cit.: 


Coal 

Bone  coal 

Coal 

Soft  coal. 

Slate  

Coal 

Slate  

Coal 


Ft.  in. 

1 2 ' 
0 2 
4 0 


u o 

2 1 

0 1 

1 11  . 


Ft. 

10 


According  to  Orton  this  bed  changes  in  character  from  a good  coking 
coal  in  eastern  Ohio  to  an  open-burning  one  from  New  Lexington  south- 
westward.  The  reader  will  find  the  coal  fully  described  in  Yol.  Y,  Ohio 
Geology. 

The  interval  separating  the  Middle  Kittanning  coal  from  the  Lower 
Kittanning  bed  varies  greatly  both  in  thickness  and  composition  in  the 
different  regions  of  the  Appalachian  field.  In  western  Pennsylvania 
and  eastern  Ohio  the  interval  is  usually  only  20  to  30  feet  and  generally 
occupied  with  dark  slates  or  shales  holding  iron  nodules,  and  it  seldom 
surpasses  40  feet  anywhere  in  Pennsylvania,  while  in  northern  West 
Yirginia  it  locally  thins  away  to  an  insignificant  parting,  but  to  the 
south  westward  in  the  Great  Kanawha  region,  and  from  there  across  to 
the  Big  Sandy,  it  often  swells  up  to  100  feet  and  occasionally  attains  a 
thickness  of  165  feet  (Section  115),  with  some  massive  sandstone  at 
several  horizons.  In  southwestern  Ohio  a massive  sandstone  30  to  40 
feet  thick  often  occupies  the  interval  to  the  exclusion  of  shales. 

In  the  Great  Kanawha  region  a siliceous  limestone  makes  its  appear- 
ance in  this  interval  and  seems  to  have  quite  a wide  distribution  in  that 
region  and  southwestward  to  the  Big  Sandy.  It  is  well  exposed  near 
the  mouth  of  Campbell’s  Creek,  and  I have  designated  it  the  Campbell’s 
Creek  limestone  from  that  locality.  This  stratum  seems  to  be  present 
even  in  northern  West  Yirginia,  since  in  Sections  95  and  96,  at  Moats- 
vi  lie  and  Yalley  Falls,  respectively,  a bed  of  siliceous  limestone  occurs 
20  feet  above  the  Lower  Kittanning  coal. 

Along  the  Tug  Fork  of  Big  Sandy  there  are  siliceous  limestones  at 


WHITE.] 


THE  LOWER  KITTANNING  COAL. 


169 


several  horizons  above  the  Campbell’s  Creek  bed,  as  shown  in  Section 
119,  there  being  two  and  sometimes  three  within  the  horizon  of  the 
Lower  Freeport  sandstone,  so  that  these  must  not  be  confounded  with 
the  one  in  question. 

The  bottom  layers  of  this  shale  interval  immediately  above  the  Lower 
Kittanning  coal  are  nearly  always  filled  with  fossil  plants.  They  occur 
in  great  variety  and  abundance  wherever  the  rock  material  in  the  roof 
of  the  underlying  coal  is  a shale,  and  this  is  the  horizon  par  excellence 
for  the  collector  of  plants  from  the  Lower  Coal  Measures. 

These  beds  have  been  thoroughly  explored  at  only  one  locality  in  the 
Appalachian  field,  viz,  Cannelton,  Beaver  County,  Pennsylvania,  where 
Mr.  I.  F.  Mansfield  has  collected  systematically  for  Prof.  Lesquereux 
during  several  years,  the  results  of  which  are  recorded  in  Report  P, 
Yols.  I and  II,  Second  Geological  Survey  of  Pennsylvania.  The  list 
includes  a large  number  of  species,  several  of  which  are  peculiar  to 
that  locality. 

THE  LOWER  KITTANNING  COAL. 

The  next  lower  bed  of  this  series,  though  formerly  named  simply 
the  Kittanning  coal  by  Rogers,  is  now  called  the  Lower  Kittanning. 
Although  seldom  attaining  any  unusual  thickness,  it  is  probably  the 
most  persistent  bed  in  the  entire  Appalachian  field,  and  has  a workable 
thickness  over  a larger  area  than  any  other.  In  Pennsylvania  it  fur- 
nishes from  3 to  4 feet  of  valuable  fuel  over  large  areas  in  every  county 
where  its  outcrop  is  due.  Of  course,  like  all  other  coals,  it  thins  down 
locally  and  becomes  worthless  over  considerable  areas,  but  the  barren 
patches  on  the  horizon  of  the  Lower  Kittanning  bed  are  fewer  and 
smaller  than  those  at  the  horizon  of  any  other  coal  in  the  entire  Lower 
Coal  Measures.  If  the  Middle  Kittanning  is  the  more  important  coal 
in  Ohio,  the  Lower  surpasses  it  in  Pennsylvania  and  West  Virginia, 
so  that  the  difference  in  favor  of  the  former  in  Ohio  is  much  more 
than  offset  in  the  latter  two  States.  This  coal  is  also  a composite  seam, 
and  when  it  acquires  considerable  thickness  is  often  split  into  several 
divisions  by  separating  slates.  In  the  Pennsylvania  field  these  slates 
are  usually  mere  knife  edges,  and  add  but  little  to  the  total  thickness 
of  the  bed,  except  in  the  eastern  portion  of  the  field,  where  in  Clear- 
field, Bedford,  and  Huntingdon  it  often  has  a layer  of  impure  fire  clay 
or  gray  shale  separating  the  bottom  member  from  the  middle  one. 

The  u Fulton  vein  ” of  the  Broad  Top  field  appears  to  be  identical 
with  this  coal,  though  the  writer  was  formerly  inclined  to  regard  it  as 
identical  with  the  Clarion  (see  T3,  Second  Geological  Survey  of  Penn- 
sylvania), and  bed  “A”  of  the  Tipton  Run  series  is  probably  the  same. 

The  u Bloss  vein”  of  Tioga  County  seems  to  be  referable  to  this  same 
horizon  both  with  reference  to  structure  and  its  position  in  the  column 
of  rocks  (Sections  50  and  51). 

In  the  Georges  Creek  field  of  Maryland  this  is  often  known  as  the 
u 6-foot”  bed,  and  its  structure  there  is  given  in  Section  92.  From  Elk 


170 


THE  NORTHERN  BITUMINOUS  COAL  FIELD. 


[BULL.  65. 


Garden  southward  along  the  North  Potomac  to  where  this  bed  passes 
under  draiuage  level,  near  Gorman,  it  is  so  badly  split  up  with  slate  as 
to  be  rather  valueless,  but  where  it  emerges  to  daylight  again  on  the 
other  side  of  the  Cheat-Potomac  divide,  near  Thomas,  it  has  become  a 
splendid  vein  nearly  11  feet  thick,  as  shown  in  Section  94,  from  which 
0 feet  of  excellent  coal  is  miued  without  taking  out  the  bottom  member. 
As  already  stated,  the  bed  attains  its  great  thickness  in  this  region  by 
the  thinning  away  of  the  shales  which  usually  separate  the  Middle  and 
Lower  Kittanning  beds,  thus  permitting  the  two  practically  to  unite 
into  one.  The  coal  from  it  here  is  prized  for  smithing  purposes  quite 
as  highly  as  the  celebrated  Blossburg  bed,  with  which  it  appears  to  be 
identical.  It  has  also  been  successfully  coked  in  this  Tucker  County 
field,  since  it  is  nearly  always  a good  coking  coal  everywhere. 

Section  at  Newburg,  Preston  County,  West  Virginia . — In  the  deep  shaft 
at  Newburg,  Preston  County,  West  Virginia,  the  Lower  Kittanning  has 
the  following  structure: 

Ft.  in. 


Coal 

Shale,  gray 

Coal 

Bony  coal . . 

Coal 

Black  slate 
Coal  


0 10  ^ 

0 10 

o 6 J Ft.  in. 
0 3 > 9 & 
4 6 ’ 

0 6 
2 0 


Sections  95  and  96  show  the  structure  of  this  bed  where  it  is  brought 
to  the  surface  by  the  Chestnut  Bidge  anticlinal,  on  the  Tygart’s  Valley 
Kiver,  below  Grafton,  West  Virginia,  and,  as  will  be  seen,  it  is  there 
about  5 feet  thick. 

On  the  Great  Kanawha  Biver,  above  Charleston,  this  is  one  of  the 
principal  coal  beds,  and  has  long  been  known  there  as  the  CampbelPs 
Creek  vein.  At  this  locality  on  CampbelPs  Creek  the  coal  is  4 to  6 feet 
thick  with  only  two  parting  slates,  but  in  passing  southward  up  the 
Kanawha  new  partings  come  in  and  the  old  ones  thicken  up  until  the 
bed,  with  its  included  rock  partings,  swells  out  to  a thickness  of  nearly 
50  feet,  and  two  of  the  members  are  mined  independently,  the  upper 
one  being  known  as  the  Peerless  bed  and  the  lower  one  as  the  Blacks- 
burg. The  upper  member  never  exceeds  3 feet,  and  is  usually  about 
20  feet  above  the  Blacksburg  member,  which  is  often  4 to  5 feet  thick 
and  is  the  “ Coal  Valley  gas  vein.”  On  the  Mount  Carbon  property,  25 
miles  south  from  CampbelPs  Creek,  the  20  feet  of  shales  which  usually 
separate  the  Peerless  and  Blacksburg  members  of  the  Lower  Kittan- 
ning coal  thin  away  to  a few  inches  locally,  and  both  are  taken  out  of 
the  same  drift.  This  is  also  the  condition  of  affairs  at  the  famous 
Austead  mines  of  the  Hawk’s  Nest  Coal  Company  on  top  of  Gauley 
Mountain.  At  the  head  of  Cabin  Creek,  a tributary  from  the  south 
bank  of  the  Big  Kanawha,  the  Peerless  and  upper  half  of  the  Blacks- 
burg member  couie  completely  together,  forming  a bed  of  excellent  gas 
coal  5£  feet  thick. 


WHITE.] 


THE  KITTANNING  FIRE  CLAY. 


171 


In  Wyoming  County,  West  Virginia,  this  coal,  which  is  locally  called 
the  “ Cook  vein,”  has  a good  development,  the  whole  seam  with  its  part- 
ing slates  being  about  25  feet  thick,  as  may  be  seen  from  Section  117, 
but  the  main  portion  of  the  bed  is  about  7 to  8 feet  thick,  separated  into 
three  layers  by  slate  partings  of  4 to  6 inches  thick. 

This  coal  rises  above  the  level  of  the  Tug  Fork  of  Big  Sandy  about  3 
miles  below  Warfield  and  30  above  Louisa.  It  has  been  mined  to  some 
extent  for  local  use  at  Warfield,  and  is  known  in  that  region  as  the 
“ Warfield  coal.”  Its  structure  there  is  given  by  Section  119.  Above 
Warfield  it  dips  down  under  the  stream  and  does  not  come  up  again  for 
about  10  miles,  or  some  distance  above  the  mouth  of  Pigeon  Creek,  but 
from  there  on  up  Tug  Biver  it  is  constantly  accessible  for  about  40 
miles,  until  the  southward  rise  of  the  rocks  throws  the  coal  above  the 
tops  of  the  hills  near  the  mouth  of  Ben  Creek,  95  miles  above  the  mouth 
of  Tug.  Along  this  line  the  coal  is  seldom  less  than  3 feet  thick  and 
frequently  4 to  5 feet,  with  only  one  slate  parting  3 to  5 inches  thick.  At 
the  mouth  of  Lick  Creek  and  60  miles  from  Louisa  this  coal  is  100  feet 
above  the  river,  and  reported  6 to  7 feet  thick,  with  only  one  thin  slate 
near  the  center. 

In  Ohio  the  Lower  Kittanning  coal  is  almost  as  persistent  as  in  Penn- 
sylvania, rarely  being  absent  entirely  from  the  section,  and  generally 
having  a thickness  of  3 feet,  with  a maximum  of  5. 

In  the  deep  oil-borings  across  southwest  Pennsylvania  and  northern 
West  Virginia  this  coal  is  quite  persistent,  being  frequently  reported  at 
a depth  of  1,500  to  1,800  feet  beneath  the  surface. 

Trie  following  list  of  names  has  been  given  it  in  Ohio  : Coal  No.  3 in 
Ohio  Valley  and  along  Yellow  Creek,  No.  4 at  Leetonia,  No.  5 in  Stark 
County  and  south  westward ; also  “ Creek  vein,”  “ Potter’s  vein,”  “ Lee- 
tonia,” “ Mineral  Point,”  “Lower  New  Lexington,”  “Newcastle,”  etc. 
This  coal  is  often  neglected  in  Ohio  even  when  it  has  a thickness  of  2J 
to  3 feet,  because  of  the  great  development  of  the  Middle  Kittanning 
coal  only  a few  feet  above.  Both  of  these  beds  have  now,  through  the 
labors  of  Newberry,  Orton,  Boy,  and  others,  been  traced  from  the  Penn- 
sylvania line  clear  across  Ohio  to  where  they  pass  into  Kentucky  at 
Ironton,  and  have  been  so  well  described  by  Orton  in  Vol.  V,  Ohio 
Geology,  that  it  is  unnecessary  for  the  writer  to  dwell  on  them  longer. 

THE  KITTANNING  FIRE  CLAY. 

Lying  directly  under  the  last  described  coai  there  comes  in  many 
regions  a great  bed  of  splendid  fire  clay  which  often  overshadows  the 
coal  in  value,  since  many  millions  of  dollars  are  invested  in  manufac- 
turing the  several  lines  of  articles  which  can  be  made  from  this  clay. 
The  bed  has  been  named  from  Kittanning,  where  it  is  mined,  and  here 
as  well  as  at  many  localities  in  Ohio  the  clay  does  not  all  immediately 
underlie  the  coal,  but  some  of  it  is  found  a few  feet  lower  and  nearly 
on  top  of  the  Ferriferous  limestone. 


172  THE  NORTHERN  BITUMINOUS  COAL  FIELD.  {bull.  65. 

Eastward  from  the  Alleghany  River  this  clay  does  not  appear  to  be 
very  important,  bat  westward  from  that  point  it  is  generally  present, 
and  attains  its  maximum  development  along  the  Beaver,  and  westward 
from  there  down  the  Ohio;  the  famous  potteries  at  New  Brighton,  Roch- 
ester, East  Liverpool,  New  Cumberland,  and  other  points  in  these  val- 
leys all  deriving  their  clay  from  this  horizon. 

In  the  Beaver  County  region  the  thickness  is  generally  about  8 to  10 
feet,  but  occasionally  runs  up  to  15  and  down  to  5.  It  often  consists  of 
two  portions,  an  upper  “ soft”  clay  and  a lower  “hard”  clay,  the  latter 
being  used  in  the  manufacture  of  fire  brick,  etc.  In  western  Pennsyl- 
vania and  eastern  Ohio  this  clay  bed  is  often  a very  valuable  element 
in  settling  questions  of  stratigraphy  which  would  otherwise  be  extremely 
difficult  of  solution  ; in  fact  it  is  valuable  for  this  purpose  clear  across 
the  Ohio  coal  field,  since,  according  to  Orton,  although  not  entirely  per- 
sistent, yet  it  furnishes  valuable  clay  mines  in  every  county  of  its  out- 
crop from  the  Pennsylvania  line  across  to  the  Kentucky  border. 

In  West  Virginia  (except  along  the  Upper  Ohio  River)  the  deposit  is 
seldom  of  value,  being  too  siliceous,  and  it  has  been  developed  in  only  one 
region,  viz,  near  the  locality  of  Section  97,  at  Ruzuuds,  on  the  Tygartfs 
Valley  River.  Here  along  the  crown  of  the  Chestnut  Ridge  anticlinal 
the  coal  above  locally  disappears,  and  then  a valuable  bed  of  hard  clay 
replaces  it,  but  when  the  coal  comes  in  again  the  clay  disappears,  just 
as  it  often  does  in  Ohio,  when  the  hard  flinty  clay  is  present.  The 
Glade  Fire  Brick  Works  at  Kuzums  manufacture  a good  fire  brick  from 
this  bed. 

THE  KITTANNING  SANDSTONE. 

The  interval  between  the  Lower  Kittanning  coal  and  the  Ferriferous 
limestone  varies  greatly  in  thickness,  sometimes  only  the  clay  bed  just 
described  intervening,  and  again  the  interval  thickens  up  to  50  to  75 
feet  or  even  more.  Whenever  the  interval  attains  anything  like  these 
last  figures  we  generally  find  a massive  sandstone  between  the  coal  and 
the  limestone,  and  to  this  has  been  given  the  name  Kittanning.  It 
sometimes,  as  on  Buffalo  Creek,  Butler  County,  Pennsylvania,  develops 
into  a great  cliff  rock  of  massive  and  even  pebbly  sandstone,  cutting  out 
the'underlying  limestone  (Ferriferous).  It  often  furnishes  good  quarry 
stone,  and  a rock  occupying  this  horizon  in  the  series  has  been  quarried 
and  used  in  building  the  Government  lock  and  dam  near  Coal  Valley, 
on  the  Great  Kanawha  River.  In  this  region  the  interval  between  the 
Lower  Kittanning  coal  and  the  Ferriferous  limestone  thickens  up  to  150 
feet,  and  a local  bed  of  coal,  the  Brownstown,  comes  into  the  series 
about  half  way  in  the  interval.  In  Wyoming  County  and  westward 
from  there  the  Kittanning  sandstone  thickens  to  100  feet,  as  seen  in 
Section  117. 

THE  BUHRSTONE  IRON  ORE. 

Resting  immediately  on  top  of  the  Ferriferous  limestone  there  occurs 
over  a very  wide  area  a deposit  of  iron  ore.  In  Pennsylvania  it  is  often 


WHITE.] 


THE  FERRIFEROUS  LIMESTONE. 


173 


underlaid  with  cherty  material,  and  hence  long  ago  received  the  name 
of  “Buhrstone  ore,”  but  it  is  there  also  called  Ferriferous  ore.  In  Ohio 
it  has  a wide  distribution  and  is  known  under  several  names,  among 
which  are  “ Baird”  ore,  “ Gray”  ore,  u Limestone”  ore. 

The  ore  generally  lies  in  immediate  contact  with  the  limestone,  in  a 
slab-like  sheet  one-half  to  1 foot  thick,  but  occasionally,  as  in  Lawrence 
County,  Pennsylvania,  on  the  Houck  farm,  it  locally  thickens  up  to  20 
feet,  entirely  replacing  the  underlying  limestone,  while  again  it  is  absent 
over  wide  areas,  or  represented  by  nodules  scattered  through  the  over- 
lying shales.  When  the  Ferriferous  limestone  is  absent,  its  place  in 
the  series  can  often  be  correctly  assigned  from  the  existence  of  this  ore, 
as  is  the  case  in  Section  97,  at  Nuzum’s  Mills,  West  Virginia.  This  bed 
was  formerly  the  main  ore  from  which  the  charcoal  furnaces  of  western 
Pennsylvania  drew  their  supplies,  and  it  is  still  the  main  feeder  for  these 
furnaces  in  southern  Ohio.  In  northern  West  Virginia  some  iron  ore 
occurs  at  this  horizon  in  Monongalia  and  Preston  Counties,  and  a few 
inches  of  it  may  be  seen  near  the  coke  ovens  on  Glady  Fork,  below 
Thomas,  Tucker  County,  but  in  the  Great  Kanawha  region  and  south- 
ward toward  the  Big  Sandy  it  appears  to  be  completely  absent  as  a 
distinct  stratum,  though  nodules  of  iron  sometimes  come  at  this  horizon. 

THE  FERRIFEROUS  LIMESTONE. 

The  occurrence  of  the  iron  ore  just  described  resting  upon  a bed  of 
limestone  over  a wide  area  suggested  the  name  4 ‘Ferriferous”  which 
the  early  geologists  applied  to  the  limestone  as  well  as  the  ore. 

Tins  is  the  most  important  and  widely  distributed  limestone  of  the 
entire  Coal  Measure  column,  important  both  in  an  economic  sense  and 
as  a strati  graphical  horizon  which  with  ordinary  care  can  be  unfailingly 
recognized  by  geologists  as  well  as  anyone  else  interested  in  determin- 
ing the  correct  order  of  the  rocks.  It  differs  from  the  other  limestones 
that  we  have  had  so  far  in  the  Lower  Coal  Measures,  in  being  a genuine 
marine  deposit,  abounding  in  fossil  criuoids,  corals,  brachiopods,  la- 
mellibranchs,  univalves,  etc.,  a list  of  the  more  common  forms  of  which 
is  given  on  pages  46  and  47,  Report  QQ,  Second  Geological  Survey  of 
Pennsylvania. 

In  Pennsylvania  this  limestone  is  confined  to  the  counties  west  from 
Chestnut  Ridge,  attaining  its  maximum  development  in  Clarion,  Arm- 
strong, Butler,  Beaver,  and  Lawrence,  where  it  is  frequently  25  feet 
thick,  or  even  more,  and  seldom  less  than  10  except  it  has  locally 
thinned  away  entirely. 

This  limestone  enters  Ohio  at  Lowellville  on  the  Mahoning  River  with 
a thickness  of  15  feet,  but  westward  it  changes  very  much  from  its 
Pennsylvania  type,  becoming  reduced  in  thickness,  sometimes  entirely 
absent,  and  occasionally  splitting  into  two  beds  separated  by  15  to 
50  feet  of  shales,  the  lower  one  of  which  has  been  called  the  Putnam 
Hill  limestone  from  its  occurrence  in  an  eminence  of  that  name  at 


174 


THE  NORTHERN  BITUMINOUS  COAL  FIELD, 


[BULL.  05. 


Zanesville.  In  one  way  or  another,  however,  it  has  been  satisfactorily 
traced  by  Orton  across  the  Ohio  field  to  where  it  enters  Kentucky  from 
Hanging  Kock. 

A layer  of  flint  or  u buhrstone”  is  often  incorporated  with  the  top  of 
this  bed  in  Pennsylvania,  and  the  same  thing  holds  true  for  Ohio,  but 
below  this  the  rock  is  generally  gray  for  10  to  15  feet  and  of  great  pur- 
ity, being  especially  prized  as  a flux  in  the  smelting  of  iron  ore,  and 
used  almost  exclusively  for  this  purpose  in  the  Pittsburgh  region.  The 
lower  portion  of  the  stratum  is  generally  of  a bluish  color,  and  its  layers 
are  slialy,  being  interstratified  with  thin  films  of  clay  and  other  impuri- 
ties, and  occasionally  a distinct  bed  of  shale  separates  the  blue  layers 
from  the  gray  above.  Hence  it  seems  very  probable  that,  as  Prof. 
Orton  once  suggested,  this  shale  layer  probably  increases  in  thickness 
through  some  regions  of  Ohio,  thus  separating  the  upper  portion,  as  the 
il  Gray  w limestone,  from  the  io  wer  or  blue  part,  which  has  been  called  the 
Putnam  Hill.  On  one  point,  however,  in  this  connection,  the  writer  can- 
not fully  agree  with  Prof.  Orton,  and  that  is  concerning  the  presence 
of  workable  coal  beds  between  these  two  divisions  of  the  limestone. 
There  is  certainly  none  at  Zanesville,  the  typical  locality  for  the  Put- 
nam Hill  limestone  (Section  104),  neither  is  there  any  at  Shawnee  (Sec- 
tion 105),  nor  at  Kew  Lisbon  (Section  103),  nor  Sprucevale  (Section 
102),  so  that  it  appears  more  probable  that  the  supposed  workable  coal 
between  the  two  layers  of  the  limestone  is  founded  upon  an  error  in 
identification. 

Another  characteristic  of  this  limestone  is  that  when  it  becomes  thin 
and  impure  it  almost  always  exhibits  the  u cone-in-cone v structure, 
though  there  are  other  horizons  in  the  Coal  Measures  which  show  the 
same  feature,  notably  the  Mercer  limestones. 

The  most  northern  point  at  which  this  limestone  has  been  found  in 
Pennsylvania  is  in  the  southern  portion  of  McKean  County,  where 
Mr.  Ashburner  identifies  with  it  a siliceous  limestone  occurring  in  the 
vicinity  of  Clermont. 

In  the  Korth  Potomac  coal  basin  this  limestone  has  been  seen  by  the 
writer  near  Gorman,  Garrett  County,  Maryland,  and  also  below  Thomas, 
along  Glady  Fork  of  Black  Water.  In  each  case,  however,  the  deposit 
is  entirely  difierent  from  the  marine  type  of  western  Pennsylvania  and 
Ohio,  and  resembles  more  the  fresh  water  limestones  under  the  Free- 
port coals,  since  no  marine  fossils  were  observed  at  either  locality;  in 
fact  there  is  no  point  in  West  Virginia  or  Maryland  where  the  marine 
type  of  this  limestone  is  known  to  exist,  so  far  as  the  writer  is  aware. 

Along  the  Great  Kanawha  Kiver,  in  the  vicinity  of  Cannelton,  a bed 
of  siliceous  limestone  occurs  75  to  100  feet  under  the  Lower  Kittanning 
coal,  and  it  has  been  identified  with  the  Ferriferous  limestone  horizon 
as  shown  in  Section  115.  It  occasionally  exhibits  the  u cone-in-cone  n 
structure  but  is  not  fossil iferous. 

Immediately  under  the  Ferriferous  limestone  in  western  Pennsyl- 


WHITE.] 


THE  CLARION  COAL. 


175 


vania  there  are  often  5 to  10  feet  of  black  fossiliferous  shales,  especially 
when  the  limestone  is  thin  or  locally  wanting,  so  that  the  horizon  can 
thus  be  frequently  recognized  without  the  presence  of  the  limestone 
since  the  fossils  in  the  shales  are  practically  the  same  as  in  the  latter. 

THE  CLARION  COAL. 

Mr.  H.  Martyn  Chance  has  recently  shown  (VV,  Second  Geological 
Survey  of  Pennsylvania)  that  the  coal  bed  which  comes  so  close  under 
the  Ferriferous  limestone  in  western  Pennsylvania,  and  was  formerly 
called  the  Scrub-grass  coal,  is  really  an  off-shoot  from  the  Clarion,  and 
hence  it  is  unnecessary  to  retain  the  name  Scrub-grass,  which  should 
be  replaced  with  Upper  Clarion. 

The  main  bench  of  the  Clarion  coal  occurs  through  western  Pennsyl- 
vania at  an  interval  of  10  to  30  feet  below  the  Ferriferous  limestone. 
Its  usual  thickness  is  about  3 feet,  though  it  often  swells  to  4 or  5. 
When  well  developed  it  generally  contains  one  or  two  parting  slates,  and 
one  of  them  thickening  up  causes  the  upper  bench  to  approach  the  Fer- 
riferous limestone,  and  it  was  then  taken  for  a separate  coal  by  the 
geologists  of  the  First  Pennsylvania  Survey,  but,  as  Chance  suggests, 
this  should  be  called  the  Upper  Clarion  bed  in  view  of  its  origin.  This 
upper  member  is  thick  enough  to  mine  in  only  a limited  area  around 
the  northern  outcrop  of  the  same  in  Clarion,  Butler,  and  Jefferson. Coun- 
ties. 

The  Lower  or  main  Clarion  bed  is  of  considerable  importance  m Penn- 
sylvania, and  generally  furnishes  some  areas  of  good  fuel  in  nearly 
every  county  where  its  outcrop  occurs,  though  as  a rule  the  coal  is 
rather  high  in  both  ash  and  sulphur. 

In  eastern  Ohio  this  bed  acquires  some  importance  in  the  vicinity  of 
Leetonia  and  New  Lisbon,  and  is  there  often  parted  by  a vein  of  tire 
clay  1 to  4 feet  thick,  the  upper  coal  alone  being  mined,  and  varying  in 
thickness  from  2J  to  3J  feet.  Prof.  Orton  has  also  shown  that  the  Can- 
field  cannel  of  Mahoning  County  belongs  to  the  horizon  of  the  Clarion 
bed. 

Westward  from  the  eastern  tier  of  Ohio  counties,  the  Clarion  coal 
disappears  according  to  Orton  and  is  of  no  more  importance  until  Vin- 
ton and  Jackson  are  reached,  but  this  conclusion  is  based  upon  his  pres- 
ent view  of  the  Putnam  Hill  limestone,  which  he  once  regarded  as  a 
“ split”  from  the  Ferriferous  of  Pennsylvania,  but  which  he  now  ap- 
pears to  reject,  since  he  puts  the  Clarion  coal  between  this  latter  lime- 
stone and  the  upper  or  “ Gray”  one,  and  identifies  the  coal  underlying 
the  Putnam  Hill  limestone  as  the  Brookville  bed  of  Pennsylvania.  The 
writer  has  elsewhere  expressed  his  doubt  of  the  existence  of  any  work- 
able coal  between  these  two  limestones,  believing  that  the  identifica- 
tions on  which  the  conclusion  was  founded  are  erroneous,  so  that  if  we 
substitute  Clarion  coal  for  “Brookville”  in  Prof.  Orton’s  Ohio  series, 


176 


THE  NORTHERN  BITUMINOUS  COAL  FIELD. 


IbulIj.  65. 


all  difficulties  concerning  the  disappearance  of  the  Clarion  coal  between 
eastern  Ohio  and  Perry  County  vanishes,  and  the  Clarion  becomes  one 
of  the  regular  and  persistent  beds  of  the  series  clear  across  Ohio  as  it 
does  in  Pennsylvania.  In  the  Zanesville  Section  (104)  the  writer  has 
indicated  his  views  as  to  the  equivalency  of  these  members  of  the  Ohio 
series. 

The  Clarion  coal  attains  its  maximum  thickness  in  Stark  County, 
Ohio,  where  it  is  6 feet  thick  and  a very  fair  steam  coal,  according  to 
Orton. 

In  northern  West  Virginia  this  bed  is  generally  present  in  the  section, 
but  is  usually  slaty  and  too  impure  to  be  valuable,  so  that  it  has  never 
been  mined  in  that  part  of  the  State. 

Section  near  Eagle,  Fayette  County , West  Virginia. — Along  the  Great 
Kanawha  Kiver  a coal  bed,  which  appears  to  come  at  this  horizon,  has 
been  largely  developed  for  coking  purposes  in  the  vicinity  of  Eagle, 
Fayette  County,  and  hence  is  locally  known  as  the  Eagle  vein.  Where 
best  developed  there,  it  varies  from  3J  to  4J  feet  in  thickness,  and  is  a 
splendid  coking  coal,  having  the  following  structure  in  the  vicinity  of 
Eagle : 


Ft. 

in. 

Coal 

1 

Shale 

0 

3I 

Ft. 

in. 

Coal 

0 

-3i 

f 4 

9 

Shale 

0 

3 

! 

Coal 

2 

10  J 

In  passing  up  the  Kanawha  from  Eagle  the  upper  shale  parting  of 
this  bed  gradually  thickens  till  at  the  mouth  of  Armstrong  Creek,  3 
miles  above,  it  becomes  20  feet  thick  and  the  coal  has  the  structure  given 
in  Section  115. 

The  interval  between  this  bed  and  the  Lower  Kittanning  varies  be- 
tween 120  and  200  feet  along  the  Great  Kanawha,  thickening  up  to  the 
latter  figures  at  Brownstown  (Section  114),  but  southward  from  this  in 
Wyoming  County  the  interval  swells  still  further  to  230  feet  in  the  vi- 
cinity of  Oceana,  as  shown  in  Section  117,  wThere  the  coal  in  question 
has  a thickness  of  5 to  6 feet  and  is  known  as  the  “ coking w vein. 
There  is  evidently  a wide  area  of  this  coal  between  the  Kanawha  and 
Big  Sandy  Bivers  in  which  it  will  prove  a valuable  coking  coal. 

A bed  of  excellent  fire  clay  often  underlies  the  Clarion  coal  both  in 
Pennsylvania  and  Ohio,  being  second  in  value  only  to  the  Kittanuing 
clay  above,  and  often  rivaling  it  in  thickness. 

The  interval  below  the  clay  down  to  the  next  coal  bed  (Brookville) 
varies  greatly  both  in  thickness  and  in  the  rock  material  which  occu- 
pies it.  Occasionally  the  series  ends  with  the  Clarion  underclay,  which 
rests  immediately  on  top  of  the  next  lower  or  Conglomerate  Measures, 
while  again,  shales  and  a sandstone  termed  by  Chance  the  Clarion 
sandstone  occupy  this  interval,  which  in  Pennsylvania  is  seldom  more 
than  30  to  50  feet  thick. 


WHITTS.  J 


THE  EAGLE  LIMESTONE. 


177 


In  Ohio  the  interval  below  the  Clarion  clay  down  to  the  top  of  the 
Pottsville  Measures  is  seldom  more  than  30  feet,  the  same  being  true 
in  northern  West  Virginia,  as  may  be  seen  from  Sections  96  and  97. 

On  the  Great  Kanawha  River  the  internal  from  the  Clarion  or  Eagle 
coal  down  to  the  top  of  the  Pottsville  Measures  thickens  to  nearly  300 
feet,  and  consists  of  a succession  of  shales  and  sandstones,  in  which 
occur  two  thiu  limestones  and  two  or  three  thin  coal  beds.  Rone  of 
the  latter  attain  a thickness  of  3 feet,  however,  anywhere  between  the 
Kanawha  and  Big  Sandy  Rivers,  so  that  the  workable  coals  of  this 
series  in  that  region  really  end  with  the  Clarion  (Eagle)  bed. 

Two  or  three  rocks  in  this  interval  of  300  feet  in  southwestern  West 
Virginia  require  more  particular  notice.  One  of  them,  and  the  upper- 
most, is  a very  pure  seam  of  coal,  which  at  Eagle  comes  only  20  feet 
below  the  main  Eagle  bed,  and  is  1J  feet  thick.  I have  termed  it  the 
Little  Eagle  coal,  since  it  is  possibly  a “ split”  from  the  main  bed 
above.  To  the  south  it  appears  to  be  quite  persistent,  since  it  occurs 
in  Wyoming  County  in  every  section;  but  the  interval  separating  it 
from  the  Eagle  bed  has  there  swelled  to  65  feet  (Section  117)  and  the 
coal  has  thickened  to  27  inches  of  the  same  excellent  fuel  as  on  the 
Kanawha. 

THE  EAGLE  LIMESTONE. 

Another  rock  worthy  of  mention  in  this  Kanawha  series  is  an  impure 
limestone  which  occurs  near  Eagle  at  an  interval  of  75  feet  under  the 
Eagle  coal.  It  is  only  about  1 foot  thick,  quite  dark,  fossiliferous,  and 
exhibits  the  “ cone-in-cone”  structure  to  a wonderful  degree,  being 
locally  known  as  u black  marble.”  The  stratum  is  immediately  under- 
laid by  dark  shales,  which  are  crowded  with  marine  fossils  of  the  same 
type  as  those  found  in  connection  with  the  Ferriferous  limestone  in 
Pennsylvania  and  Ohio ; in  fact,  so  many  of  the  species  are  identical,  and 
the  limestone  itself  so  closely  resembles  the  Ferriferous  when  thin,  that 
sometimes  I have  been  inclined  to  think  that  the  two  beds  may  possibly 
be  identical,  though  this  would  seem  to  be  impossible  from  the  structure 
of  Section  115,  in  which  the  whole  lower  coal  series  is  exposed  both 
above  and  below  this  stratum.  If  it  should  turn  out  to  be  identical 
with  the  Ferriferous,  however,  then  the  Eagle  coal  would  be  the  Lower 
Kittanning,  instead  of  the  Clarion,  and  the  Campbell’s  Creek  bed  the 
Middle  Kittanning,  or  Neisonville  seam  of  Ohio,  instead  of  the  Lower 
Kittanning.  The  reader  will  understand  the  difficulty  of  correlation 
when  he  remembers  that  the  lower  coal  series  is  less  than  200  feet  thick 
in  the  Hocking  Valley,  Ohio,  while  here,  only  120  miles  southward,  the 
same  series  has  swelled  out  to  1,000  feet. 

The  fossiliferous  type  of  the  limestone  and  its  accompanying  fossilif- 
erous shale  have  never  been  seen  by  the  writer,  except  in  the  vicinity 
of  Eagle,  and  hence  I have  preferred  to  regard  it  as  a local  deposit 
below  the  horizon  of  the  Ferriferous,  since  the  fossils  of  the  Lower  Coal 
Measures  have  the  same  general  facies  at  all  horizons. 

Bull.  65 12 


178  THE  NORTHERN  BITUMINOUS  COAL  FIELD.  [bull. 65. 

THE  BROOK VILLE  COAL. 

At  the  very  base  of  the  Lower  Coal  Measures,  except  the  intervening 
underclay,  there  occurs  in  Jefferson,  Clarion,  and  some  other  counties 
of  Pennsylvania,  a bed  of  usually  slaty  and  otherwise  impure  coal, 
which  was  long  ago  named  the  Brookville  bed,  from  its  supposed  occur- 
rence near  the  town  of  that  name  in  Jefferson  County.  This  coal  ac- 
quires some  local  importance  around  the  northern  margin  of  the  coal 
field  in  Jefferson,  Clarion,  Butler,  and  Mercer  Counties,  but  southward 
and  westward  it  thins  away  and  is  often  absent  even  as  an  impure  bed, 
there  being  no  coal  whatever  at  this  horizon  where  the  Pennsylvania 
series  enters  Ohio  5 and  if  I am  correct  in  identifying  Prof.  Orton’s 
“Brookville”  coal,  (Yol.  V,  Ohio  Geology)  with  the  Clarion  of  Penn- 
sylvania, then  the  Brookville  coal  is  generally  absent,  or  at  least  sel- 
dom workable  anywhere  in  that  State. 

Yery  frequently  the  Brookville  coal  is  represented  in  Pennsylvania 
by  only  a bed  of  black  slate  or  coaly  shale,  resting  on  the  top  of  the 
Conglomerate  Measures,  and  this  is  the  case  in  northern  West  Yirginia, 
there  being  no  workable  coal  at  this  horizon  anywhere  in  that  State,  so 
far  as  the  writer  is  aware.  Even  in  the  Kanawha  field,  where  this 
lower  portion  of  the  column  is  so  greatly  thickened,  the  largest  coal 
bed  referable  to  the  Brookville  horizon  is  the  one  in  the  Wyoming 
County  section  (117),  and  this  is  only  22  inches. 

On  the  Great  Kanawha  a bed  of  very  bituminous  shale  (Section  115), 
from  which  lubricating  oil  was  once  manufactured,  may  possibly  repre- 
sent the  Brookville  coal  horizon,  since  it  is  the  lowest  bituminous 
stratum  in  the  series  there. 

Below  this  coal  in  Pennsylvania,  and  resting  immediately  on  the  top 
of  the  Conglomerate  series,  there  is  sometimes  a good  bed  of  fire  clay, 
and  Mr.  Chance  refers  to  this  horizon  the  clay  which  is  mined  so  ex- 
tensively in  Clearfield  County,  at  Blue  Ball,  Wallaceton,  and  other 
points  along  the  line  of  the  Tyrone  and  Clearfield  Railroad. 


CHAPTER  VI. 


THE  POTTSVILLE  CONGLOMERATE  SERIES. 

THICKNESS,  CHARACTER,  AND  EXTENT. 

Beneath  the  lowest  member  of  the  last  described  series  there  comes 
in  a group  of  rocks  (No.  XII)  which  are  nearly  always  so  different  from 
those  in  any  other  portion  of  the  Carboniferous  system  that  all  geologists 
have  regarded  them  as  worthy  of  being  placed  in  a distinct  series.  To 
this  series  several  names  have  been  given.  * The  early  geologists  of 
Pennsylvania  called  it  the  “ Serai”  or  “Great”  Conglomerate,  while  in 
Virginia  it  has  generally  been  named  the  No.  XII  Conglomerate,  or 
simply  No.  XII.  Prof.  Lesley  has  in  recent  years,  however,  given  it 
the  geographical  designation  of  Potts ville  Conglomerate,  from  the  great 
development  of  the  series  near  the  town  of  that  name,  while  Prof.  Fon- 
taine, following  the  Pennsylvania  custom  of  naming  the  several  coal 
series  after  prominent  rivers  along  which  the  beds  are  exposed,  has 
suggested  the  name  New  River  series,  from  that  region  of  West  Vir- 
ginia where  its  coal  beds  attain  a great  development. 

But  since  only  one  geographical  name  is  admissible  for  the  series, 
and  as  the  term  Pottsville  is  now  so  well  ingrafted  upon  geological 
nomenclature  through  the  numerous  reports  of  the  Second  Geological 
Survey  of  Pennsylvania,  it  is  thought  best  to  retain  it  for  the  series, 
and  at  the  same  time  retain  New  River  for  the  name  of  the  coal  group 
which  attains  such  prominence  along  that  stream,  thus  putting  it  on  a 
par  with  the  Mercer  group,  which  occurs  in  the  upper  portion  of  the 
series. 

As  exhibited  everywhere  in  Pennsylvania  and  West  Virginia,  this 
series  is  very  sharply  set  off  from  the  Lower  Coal  Measures  above  and 
the  Lower  Carboniferous  below,  since  in  both  cases  there  is  a great 
chauge  in  the  lithology,  so  that  the  geologist  finds  no  difficulty  in  deter- 
mining where  the  Pottsville  series  begins  as  well  as  where  it  ends. 

The  series  as  a whole  possesses  a large  amount  of  hard,  white,  or 
grayish  white  sandstone,  much  of  which  is  often  conglomeritic.  The 
sandstones  are  harder,  more  compact,  and  siliceous  than  any  in  the 
Lower  Coal  Series  above.  Bowlders  of  these  sandstones  take  a smooth 
polish  when  rolled  along  river  beds,  but  this  is  not  the  case  with  most 
sandrocks  above  this  horizon. 

The  fossil  contents  are  also  different  from  those  of  any  sandstones 
above,  since  here  for  the  first  time  in  descending  the  column  of  rocks 

179 


[bull.  65. 


180  THE  NORTHERN  BITUMINOUS  COAL  FIELD. 

do  we  find  sigillarise  and  the  large  lepidodendra  very  abundant  in 
sandstones. 

At  the  base  of  the  series  the  change  in  lithology  and  life  remains  is 
even  more  abrupt,  since  with  the  disappearance  of  the  white  or  gray 
sandstones  and  conglomerates,  limestones,  red  shales,  and  green  mica- 
ceous sandstones  appear,  in  which  plant  remains  are  rare  and  the  fossil 
trees  are  all  small. 

The  Pottsville  being  composed  mainly  of  very  hard  sandstones,  the 
grains  of  which  are  cemented  by  silica  and  peroxide  of  iron,  becomes 
almost  indestructible  by  ordinary  atmospheric  influences,  and  has  thus 
proved  a most  important  factor  in  determining  the  topography  of  the 
Carboniferous  system.  Whenever  these  beds  come  to  the  surface  in 
West  Virginia  and  Pennsylvania,  wild  and  rugged  scenery  is  sure  to 
be  found.  Eapid  rivers,  high  waterfalls,  great  cliffs,  and  barren  re- 
gipns  generally,  mark  the  lines  where  these  rocks  emerge  to  daylight. 
The  loftiest  peaks  of  the  Alleghany  Mountains  owe  their  origin  to  this 
friendly  mantle,  while  its  upturned  edges  have  preserved  many  coal 
basins  from  complete  destruction.  The  deep  gorges,  narrow  canons, 
and  wild  scenery  of  the  Alleghany,  Youghiogheny,  Cheat,  Mononga- 
hela,  New,  Guyandotte,  and  JBig  Sandy  Rivers  are  all  carved  out  of 
these  rocks.  The  Falls  of  the  Yough,  Cheat,  Tygart’s  Valley,  Kanawha, 
and  the  “Roughs”  of  the  Guyandotte  and  Big  Sandy  are  all  made  by 
these  same  beds. 

It  was  formerly  supposed  that  a vast  sheet  of  pebbly  material  under- 
laid all  of  the  true  Coal  Measures,  and  that  it  was  destitute  of  coal ; 
but  the  recent  work  of  the  Second  Geological  Survey  of  Pennsylvania 
has  shown  that  the  series  is  very  complex,  consisting  of  several  distinct 
sandstone  members,  between  which  occur  shales,  several  coal  beds,  and 
occasionally  some  limestone. 

In  Ohio  it  happens  that  the  upper  members  are  not  so  massive  as  in 
Pennsylvania  or  West  Virginia,  while  the  coal  beds  which  are  promi- 
nent only  around  the  margins  are  well  developed  there,  so  that  the 
Ohio  geologists  have  classed  the  upper  portion  with  the  Lower  Coal 
Measures,  and  retained  only  the  lowest  member  of  the  series,  viz,  a 
stratum  termed  the  Sharon  Conglomerate,  as  the  representative  of  the 
whole  series  elsewhere.  I shall  show  in  the  following  pages  that  the 
whole  series  is  easily  recognized  in  Ohio,  and  that  the  western  Penn-  - 
sylvania  type  of  these  measures  can  be  traced  across  Ohio,  and  hence  < 
for  the  sake  of  uniformity  in  nomenclature  the  Ohio  geologists  should 
cut  off  100  to  150  feet  from  the  bottom  of  their  Lower  Coal  Measure 
column  and  combine  it  with  the  Sharon  Conglomerate  below,  thus 
making  several  members  for  the  series  instead  of  a single  stratum. . 

The  coals  of  the  Pottsville  :>eries,  unlike  those  in  the  measures  above,  - 
are  persistent  and  valuable  only  around  the  margins  of  the  Appalachian 
coal  field,  and  for  the  most  part  only  where  their  outcrops  are  above 
the  level  of  the  principal  drainage  streams,  so  that  the  conditions  for- 


BULLETIN  NO.  05  PL. 


THE  POTTSVILLE  CONGLOMERATE  TOPOGRAPHY  IN  BLACKWATER  CANYON,  TUCKER  COUNTY,  WEST  VIRGINIA. 


v'  . .. 


THE  LIBRARY 
OF  THE 

UNIVERSITY  OF  ILLINOIS 


WHITE.] 


THE  POTTSVILLE  CONGLOMERATE. 


181 


merly  supposed  to  apply  to  the  Lower  Goal  Measures  do  actually  pre- 
vail with  reference  to  the  coal  in  this  series,  since  hundreds  of  carefully 
kept  well  records  testify  to  the  absence  of  any  workable  coal  beds  in 
this  series  over  all  except  the  outer  rims  of  the  Appalachian  field. 
This  same  fact  is  visible  to  the  eye  in  passing  inward  toward  the  center 
of  the  field  down  any  one  of  the  great  rivers  which  drain  into  the  Ohio. 
The  Sharon  coal  disappears  southward  along  the  Shenango  and  Mahon- 
ing rivers  long  before  its  horizon  dips  down  to  water  level]  the  New 
River  coals  fade  out  of  the  section  before  their  outcrops  touch  the 
stream  to  the  north ; the  great  bed  at  Pocahontas  does  not  extend  in- 
definitely down  the  Guyandotte  and  Tug  rivers,  but  only  20  to  30  miles, 
until  it  dwindles  away  to  a bed  too  thin  to  mine,  so  that  should  a shaft 
be  sunk  to  these  beds  30  or  40  miles  from  their  southern  or  northern 
outcrops  respectively,  the  same  massive,  pebbly,  white  sandstones 
would  be  found,  but  instead  of  inclosing  valuable  coal  beds  they  would 
hold  only  thin  streaks  of  coal  and  some  black  slates. 

Another  peculiarity  about  these  interconglomerate  coals  is  the  great 
difference  in  quality  between  those  around  the  southern  rim  of  the  Ap» 
palachian  field  and  those  around  its  northern  border,  for  in  western  Penn- 
sylvania and  across  Ohio  they  are  all  open  burning,  hard,  and  generally 
known  under  the  name  of  “ block”  coals,  which  can  be  used  in  furnaces 
in  the  raw  state,  while  to  the  south,  through  West  Virginia,  Virginia, 
and  on  into  Tennessee  and  Alabama,  these  same  coals  are  very  soft 
and  tender,  always  cementing  and  making  good  coke.  This  difference 
is  connected  with  different  conditions  of  accumulation,  there  probably 
being  less  moisture  in  the  great  peat  swamps  at  the  north,  and  the 
vegetable  accumulations  taking  place  not  under  water,  but  partially  at 
least  in  the  open  air.  This  much  would  be  indicated  by  the  innumer- 
able films  of  mineral  charcoal  which  characterize  the  northern  coals 
and  render  them  non-cementing.  To  the  unequal  rate  of  subsidence  on 
the  two  sides  of  the  Appalachian  basin  is  doubtless  owing  the  condi- 
tions which  brought  about  the  difference  in  the  character  of  the  coals. 

Another  peculiarity  is  the  great  purity  of  these  early  formed  coals, 
their  freedom  from  injurious  quantities  of  ash  and  sulphur,  both  at  the 
north  and  south.  This  also  appears  to  be  due  to  the  conditions  attend- 
ing their  deposition  rather  than  to  any  difference  in  vegetable  tissues, 
since  just  previous  to  the  spread  of  these  early  coal  marshes  the  whole 
Appalachian  region  was  sheeted  with  a thick  layer  of  clean  gravel  and 
white  sand,  thus  effectually  covering  up  the  muddy  deposits  of  a former 
epoch  and  causing  the  streams  which  drained  into  the  peat  bogs  of  that 
time  to  be  pure  and  clear  like  our  own  mountain  brooks  of  the  present. 

The  thickness  of  the  Pottsville  series  varies  greatly  in  different  por- 
tions of  the  Appalachian  basin.  In  the  bituminous  regions  of  Penn- 
sylvania, and  everywhere  in  Ohio,  they  rarely  exceed  300  feet  and  sel- 
dom go  below  150]  but  south  westward  through  West  Virginia  they 
begin  to  swell  out,  reaching  700  feet  at  the  head  of  Black  Water,  in 


182 


THE  NORTHERN  BITUMINOUS  COAL  FIELD. 


[BULL.  65. 


Tucker  County ; 1,400  on  the  New  River  in  Fayette,  and  probably 
1,800  at  the  Kentucky  line  on  the  Tug  River,  in  McDowell.  Map  Sec- 
tion C will  exhibit  the  manner  and  rate  at  which  these  beds  thicken 
southeastward  from  their  northwestern  outcrop  in  Ohio.  The  data  for 
its  construction  were  obtained  from  surface  measurements  aud  oil-well 
borings,  several  of  which  have  been  recently  made  along  the  Great 
Kanawha. 

This  series  is  also  the  repository  of  much  salt  water,  as  well  as  some 
oil  and  gas.  The  celebrated  brines  on  the  Great  Kanawha,  as  well  as 
at  Pomeroy  and  many  other  localities  along  the  Ohio  Kiver,  come  in  its 
basal  members,  while  the  “first  gas  sand”  of  the  Cannonsburg  and 
Hickory  region  of  Washington  County,  Pennsylvania,  is  found  in  the 
upper  half  of  the  same.  This  rock  is  also  gas-bearing  near  Glover’s 
Gap,  on  the  Dodd  farm,  and  near  Mannington,  Marion  County,  West 
Virginia,  on  the  Snodderly  farm. 

We  shall  now  give  a number  of  sections  in  different  portions  of  the 
Appalachian  field,  illustrating  the  character  and  thickness  of  the  Potts- 
ville  series,  and,  as  with  the  Lower  Coal  Measures,  shall  begin  at  the 
northeastern  end  of  the  field  aud  proceed  south  westward  to  the  Ken- 
tucky line. 

Section  in  Fox  Township , Elk  County , Pennsylvania. — The  following 
section  (Fig.  122)  exhibits  the  structure  of  these  beds  in  Fox  Township, 
Elk  County,  Pennsylvania,  as  given  by  Ashburner  (Keport  RR,  p.  186, 
Second  Geological  Survey  of  Pennsylvania) : 


Fig.  122.— Section 
in  Fox  Town- 
ship, Elk  Coun- 
ty, Pa. 


Fox  Township,  Elk  County,  Pennsylvania. 
[See  map,  D r.] 


1.  Sandstone,  Homewood 

( Coal 

16late,  black 

Coal 

Slate,  black 

Coal 

3.  Slate  and  fire  clay 

( Coal 

4.  Coal < Slate 

(Coal 

5.  Sandstone  Conoquenessing 

6.  Shale  and  slate 

7.  Conglomerate 

8.  Shales  of  Ho.  XI 


1'  2" 
O'  3" 
V 6" 
0'  3" 
1'  6" 


1'  8" 
3'  0" 
1'  3" 


Ft.  in . 
35 


4 8 


15 

5 11 

50 

10 

50 


Total 


170  7 


As  will  be  observed,  the  series  is  thin  iu  this  region,  and  it  seems  to 
decrease  still  more  in  Tioga  County  further  to  the  northeast,  where  it  is 
less  than  100  feet  and  all  in  one  solid  bed. 

Section  at  Clearfield , Clearfield  County , Pennsylvania. — At  the  town 
of  Clearfield,  in  the  county  of  the  same  name,  a well  was  once  bored  for 
salt.  It  begins  near  the  top  of  these  measures,  aud  the  record  shows  the 
following  structure  (Fig.  123),  as  given  in  Report  H,  Second  Geological 
Survey  of  Pennsylvania : 


WHITE.] 


Fig.  123.— Section  at 
Clearfield,  Clear- 
field County,  Pa. 


Fig.  125.  — Section 
near  Patton  Sta- 
tion, Clarion 
County,  Pa. 


THE  POTTS VILLE  CONGLOMERATE 


183 


Clearfield , Pennsylvania,  from  boring . 

I See  map,  E s.J 

1.  Sandstone,  ferruginous 

2.  Sandstone,  brown 

3.  Sandstone,  light  colored 

4.  Sandstone,  coarse,  iron-stained  

5.  Slate,  black,  mixed  with  sand 

6.  Sandstone,  iron-stained,  crumbly 

7.  Slate,  soft  gray 

8.  Sandstone,  iron-stained,  crumbly 

9.  Sandstone,  white - 

10.  Sandstone,  grayish  white 

11.  Slate,  dark 

12.  Sandstone,  light  gray 

13.  Shales,  and  red  beds  of  No.  XI. 


Ft. 

96 

4 

37 

13 

50 

15 

73 


Total. 


288 


Section  near  Brookville,  Jefferson  County , 
Pennsylvania. — In  the  vicinity  of  Brook- 
ville, Jefferson  County,  Pennsylvania, 
these  beds  exhibit  the  following  structure 
(Fig.  124),  as  learned  from  surface  obser- 
vations combined  with  the  record  of  the 
Brookville  Gas  Company’s  well  No.  2 : 

BrooTcville,  Jefferson  County , Pennsylvania. 

[See  map,  Ep.]  Ft.  in. 

1 Sandstone,  massive,  Homewood 75 

2.  Shales  and  sandstone 30 

3.  Coal  f 0 2 

4.  Fire  clay 5 

5.  Sandstone,  massive 70 

6.  Concealed 10 

7.  Sandstone,  massive 90 

8.  Slate 20 

9.  Sandstone,  hard 46 

10.  Slate 4 

11.  Sandstone,  hard 22 

12.  Red  shales  of  No.  XI. 


Total 372  2 

Here  the  series  has  thickened  consider- 
ably, and  the  triple  structure  of  its  sand- 
stones so  often  found  in  Pennsylvania  be- 
comes prominent.  N o.  4 appears  to  occupy 
the  horizon  of  the  Mount  Savage  fire  clay. 

Section  near  Patton  Station , Eed  Banlc 
Township , Clarion  County , Pennsylvania. — 


Fig.  124.— Section 
near  Brookville, 

, Jefferson  Coun* 

Near  Patton  Station,  Bed  Bank  Township,  ty,  Pa. 
Clarion  County,  Pennsylvania,  the  rocks  of  this  series 
exhibit  the  following  structure  (Fig.  125),  according  to 
Mr.  H.  Martyn  Chance  (Report  VV,  p.  116,  Second 
Geological  Survey  of  Pennsylvania) : 

Patton  Station,  Red  Bank  Township,  Clarion  County,  Pennsylvania. 


(See  map,  Eo,] 

1.  Sandstone,  hard,  massive,  Homewood 

2.  Shale,  with  a streak  of  coal 

3.  Iron  ore  bed 

4.  Shale 


5.  Sandstone 

6.  Shale,  with  kidney  iron  ore 

7.  Sandstone  and  shale 

8.  Shale,  with  sandy  layers  and  ore  bails  ... 

9.  Sandstone,  with  interbedded  thin  shales. 
10.  Red  shale. 

Total 


Feet. 

40 

20 

1 

15 

25 

35 

50 

40 

40 

266 


184 


THE  NORTHERN  BITUMINOUS  COAL  FIELD. 


[bull.  G3. 


Section  at  Keller sburg,  Armstrong  County,  Pennsylvania. — Is  ear  Kel- 
lersburg,  Armstrong  County,  Pennsylvania,  these  measures  have  the 
following  structure  (Fig.  126),  according  to  Mr.  William 
G.  Platt  (H  5,  p.  194,  Second  Geological  Survey  of 
Pennsylvania) : 


.v.v.v/.v.v. 

62' 

,-,v  .-.v.v.v.v 

/ 

10  2! 
10' 
3', 

d 

WM&M 

III! 

M 

150* 

IJillf 

2'Z'. 

10 

50' 

< 174' 


Section  at  Kellersburg,  Armstrong  County , Pennsylvania. 

[See  map,  Fo,] 

Ft.  Ft.  in. 

1.  Sandstone,  massive,  Homewood 62 1 

2.  Shales 5}- 

3.  Sandstone 10  j 

4.  Coal  (Mercer  group) 

5.  Shales  with  iron  ore 18 

6.  Fire  clay 3 

7.  Shales 3 

8.  Sandstone  (Connoquenessing) 150  J 

9.  Coal  (New  River  group) 0 2 

10.  Clay 2) 

11.  Shales 10  > 62 

12.  Sandstone 50  1 


77 


174 


Total. 


313 


Here  two  prominent  coal  horizons  are  represented  by 
mere  streaks,  the  upper  one  being  that  of  the  Mercer 
group  of  western  Pennsylvania  and  Ohio,  while  the 
lowrer  is  the  Sharon  coal  horizon  of  the  latter  States 
and  the  New  Eiver  group  of  West  Virginia. 
KdiersFurg^Arm-  Section  under  Pittsburgh , Pennsylvania. — U n d er  Pitts- 

strong  county,  Pa.  kurg]^  Pennsylvania,  we  learn  the  structure  of  this 
series  from  the  careful  record  (Fig.  127)  of  the  Jones  & Laughlin  gas 
well  No.  2,  as  given  in  the  Pennsylvania  Geological  Survey,  1886,  p.  734  : 


Fig.  127  — Section 
un  dor  Pi  ttsb  urgh , 


Under  Pittsburgh,  Pennsylvania ; boring. 

[See  map,  I m.] 


ao'  1.  Sandstone,  white,  massive,  Homewood... 

2.  Slate,  black,  trace  of  coal 

3.  Slate,  dark,  with  sand  shells 

4.  Coal  and  slate,  with  white  sandstone 

5.  Sandstone,  grayish  white,  fine 

6.  Coal,  coal  slate,  and  white  sandstone 

7.  Sandstone  and  black  slate 

8.  Sandstone,  grayish  white,  slate  in  center 

9.  Sandy  shale,  dark 

7°'  10.  Coal 

11.  Sandy  shale,  dark 

12.  Coal 

13.  Sandy  shale,  dark „ 

14.  Sandstone  and  black  slate..- 

15.  Slate,  black,  sandy,  trace  of  coal 

16.  Limestone,  Lower  Carboniferous. 


Feet. 
45) 
15  > 

20  j 


18) 
42  j> 
10  j 


Feet. 


5 

10 

70 

Trace. 

20 

1 

2 

7 

7 


Total 


207 


Section  under  Murraysville , Pennsylvania. — Under  Murraysville,  West- 
moreland County,  Pennsylvania,  the  structure  is  thus  exhibited  (Fig. 


WHITE.] 


THE  POTTSVILLE  CONGLOMERATE, 


185 


128)  by  the  record  of  the  Philadelphia  Company’s  gas  well  No.  49, 
McCutclieon  farm,  according  to  William  S.  Stevenson, 
assistant  superintendent  of  the  company: 


3y 


5<f 


.Under  Murraysville,  Westmoreland  County , Pennsylvania  (boring). 

[See  map,  I n.]  Feet. 

1.  Sandstone,  gray,  hard,  close 

2.  Slate,  black,  soft - - 

3.  Sandstone,  gray,  hard,  close 

4.  Slate,  black,  soft 

5.  Sandstone,  gray,  hard,  close 

6.  Slatp,  black,  soft - 

7.  Red  shale  of  No.  XL 


9lf 


Total. 


235 


45* 


Fig.  128. — Section  un- 
der Murraysville. 


Section  under  W ashington , Pennsylvania. — Under  Wash- 
ington, Pennsylvania,  the  structure  is  thus  given  (Fig. 
129)  by  Prof.  Linton  from  the  careful  record  he  kept  of 
the  Thayer  oil  well  (Geological  Survey  of  Pennsylvania, 
p.  765,  1886): 

Under  Washington,  Pennsylvania  (boring). 


[See  map,  J k.] 


Ft.  in.  Ft.  in. 


87 


1 6 


no  o 


iio'e* 


( Sandstone,  fine  gray 9'  ] 

1.  Sandstone,  ! Sandstone,  white  micaceous 32' ( 

Homewood  . : Sandstone,  white  and  dark  mixed. . 17'  f 

( Sandstone,  white,  fine 29' J 

2.  Coal 

3.  Sandstone,  white,  hard,  salt  water 06  0] 

4.  Sandstone,  fine,  white  and  dark  . . . .* 15  | 

5.  Shale,  very  dark,  hard  shells 13  ( 

6.  Sandstone,  white,  fine 10  ( 

7.  Shale,  black. 4 | 

8.  Sandstone,  white,  fine 2 j 

9.  Shale,  black,  and  coal 2 

10.  Sandstone,  close  grained 1 

11.  Shale  and  slate  13  > 29 

12.  Shale  and  shells 15  ) 

13.  Shale,  black,  top  of  Lower  Carboniferous  beds. 

Total 230 

Here,  as  at  Pittsburgh  (Section  127),  a careful  rec- 
ord discloses  thin  representatives  of  the  Mercer  and 
New  Eiver  coal  groups  Nos.  2 and  9,  re- 
spectively. 

Section  in  Broad  Top  basin , Huntingdon  County , Pennsyl- 
vania.— In  the  Broad  Top  basin  of  Huntingdon  County, 
Pennsylvania,  the  structure  of  these  beds  is  as  follows 
(Fig.  130),  according  to  Iteport  T3,  p.  69,  Second  Geo- 
logical Survey  of  Pennsylvania: 


Fig.  129. — Section  un- 
der Washington,  Pa. 


30' 


Broad  Top  basin,  Huntingdon  County,  Pennsylvania. 


[See  map,  1 1.] 


Fig.  130. — Section 
in  Broad  Top 
basin,  flunting- 
don  County,  Pa. 


Sandstone,  slightly  pebbly,  nomewood. 
‘ ‘ ‘ bed.... 

3.  Sandstone,  pebbly. 


2.  Shales,  with  a coal  bed- 


4.  Shales,  with  a coal 

5.  Sandstone,  pebbly. . 


Total 


Feet. 

50 

25 

50 

10 

25 

100 


The  triple  structure  of  the  sandstones  with  intervening  coal  horizons 

is  noteworthy  here. 


186 


THE  NORTHERN  BITUMINOUS  COAL  FIELD. 


[BULL.  65. 


Section  near  Weliersburg , Pennsylvania. — At  the  northern  end  of  the 
Georges  Creek  or  Cumberland  coal  basin,  near  Weliersburg,  Somerset 
County,  Pennsylvania,  these  beds  show  the  following 
structure  (Fig.  131)  in  the  gap  of  Gladden’s  Pun, 
through  the  easternmost  ridge  of  the  Alleghanies : 


143'6* 


Gladden’s  linn,  Somerset  County,  Pennsylvania. 
[See  map,  L q.] 

Ft.  in. 

1.  Sandstone,  massive,  Homewood 

2.  Coal,  Mount  Savage  

3.  Fire  clay,  Mount  Savage 7 6 

4.  Sandstone,  pebbly . .. 125 

5.  Sandstone,  dark,  shaly 10 

C.  Shale 1 

C Coal O'  1 

7.  Coal < Slate 

( Coal 

8.  Fire  clay,  impure,  sandy 10 

9.  Shales,  dark,  with  iron  ore 20 

10.  Sandstone,  massive 35 

11.  Red  beds  of  No.  XI. 


Ft.  in. 
75 
4 

143  6 


...  O'  1'') 

...  O'  4"  > — . 
..  0'  3"  ) 


0 8 


65 


Total 288  2 


20' 


This  section  shows  the  horizon  of 
the  famous  Mount  Savage  fire  clay  to 
be  in  the  Mercer  coal  group.  No.  4 
represents  the  Connoquenessing  sand- 

FigTTsl— Section  near  stones>  while  No.  7 is  probably  at  the 
Weliersburg,  Pa.  horizon  of  the  Sharon  coal. 

Section  near  Piedmont  and  Westernport , Mineral  County , 
West  Virginia.— The  Pottsville  conglomerate  beds 
thicken  very  rapidly  in  passing  southward  from  the 
Pennsylvania  line  through  Maryland  and  West  Virginia 
along  the  Alleghany  Mountain  region.  This  is  shown 
by  the  following  section  (Fig.  132),  taken  on  the  North 
Potomac,  at  Piedmont  and  Westernport,  where  that 
stream  cuts  through  the  East  Front  Eidge  of  the  Alle- 
ghanies : 


Near  Piedmont,  Mineral  County,  West  Virginia. 


[See  map,  N p.l 


Sandstone,  massive,  Homewood 

Coal 

Shales,  dark,  containing  fossil  plants . 

Sandstone,  hard,  massive 

Shales,  and  concealed . 


Ft. 


Ft. 

20 


45 1 
40  I 

30  > 127 


Sandstone,  flaggy 10 

Shale 2) 

Coal 1 

Fire  clay,  dark,  sandy 12  ) 

Sandstone,  flaggy 10  5 

Coal i. 1 

Shale,  with  nodular  iron  ore 2 > 

Shales  and  flaggy  sandstone 40  \ 87 

Sandstone,  white,  pebbly,  very  hard 45) 

Shale,  with  streaks  of  coal 5 

Concealed  shales  and  sandstones 145 1 

Sandstone,  massive 10  j 

Shales,  bituminous 10  > 195 

Sandstone,  flaggy 10 

Sandstone,  massive 20 

Coal 1 

Sandstone 4 

Fire  clay  and  shaio 3 

Sandy  shales  to  top  of  No.  XI  red  beds 4 


145' 


155* 


Total 


473 


Fig.  132.— Section 
near  Piedmont, 
Mineral  County, 
W.  Va. 


WHITE.] 


$ 


Fig.  133. — Section  a 
mouth  of  North  Fork  c 
Black  Water,  W.  Va. 


THE  POTTSVILLE  CONGLOMERATE.  187 


Section  on  Black  Fork  of  Cheat  Elver , Tucker  Coun  ty , 
West  Virginia. — In  Tucker  County,  West  Virginia, 
50  miles  soutli-soutliwest  from  Piedmont,  in  tlie  gap 
made  by  the  Black  Fork  of  Cheat  Biver  through  the 
central  portions  of  the  Alleghany  Mountains,  these 
beds  exhibit  a much  greater  thickness  than  at  Pied- 
mont, as  will  be  seen  by  the  following  section  (Fig. 
133)  made  there  by  Mr.  James  Parsons,  chief  engi- 
neer of  the  West  Virginia  Central  Bailroad : 


Mouth  of  North  Fork  of  Black  Water,  Tucker  County,  West  Vir- 
ginia. 


[See  map,  P o.] 

1.  Sandstone,  Homewood 

2.  Coal,  slaty  and  bituminous  shale 

3.  Shale,  dark 

4.  Sandstone,  massive,  pebbly 

5.  Brown  shale 

6.  Coal  (Nuttall) 

7.  Shale,  drab 

8.  Sandstone,  massive 

9.  Shales  with  iron  nodules 

10.  Fire  clay 

11.  Shale 

12.  Sandstone,  fine  grained,  flaggy 

13.  Shale 

14.  Coal 

15.  Shale 

16.  Sandstone,  massive 

17.  Sandstone  and  shales 

18.  Coal 

19.  Shale,  brown 

20.  Coal. 

21.  Bituminous  shale,  with  coal  streaks 

22.  Brown  shale e 

23.  Coal 

24.  Bituminous  shale,  with  coal  streaks 

25.  Shale 

26.  Sandstone,  massive 

27.  Shale,  brown 

28.  Red  beds,  top  of  No.  XI. 


Ft.  in.  Ft.  in. 

40 


9 

228 

26 


16 

47 

28 

2 

4 

39 

6 


j 263 
2 6 

, 142 


24 

65 

43 

0 

22 

1 

6 

26 

1 

3 

32 

35 

20 


0 6 

1 

132 


2 


59  10 


Total 733  10 

Here  we  find  the  entire  interconglomerate  coal 
group  represented.  No.  2 comes  apparently  at  the 
Mercer  horizon  and  is  the  u Railroad”  vein  along  the 
Potomac. 

No.  G comes  at  the  horizon  of  the  Nuttall  bed  of  New 
Biver,  while  Nos.  14  to  24  represent  the  lower  ones 
t along  that  stream  as  well  as  the  great  Pocahontas  vein 
of  McDowell  and  Mercer  Counties,  West  Virginia. 


188 


THE  NORTHERN  BITUMINOUS  COAL  FIELD. 


[bull.  65, 


Section  near  Rowlesburg , West  Virginia. — A fine  section  of  the  Con- 
glomerate coals  is  exposed  in  the  cuts  of  the  Baltimore  and  Ohio  Rail- 
road, near  the  summit  of  Cheat  River  grade,  4 miles  west  from  Rowles- 
burg,  Preston  County,  West  Virginia  (Fig.  134) : 


£»' 


Along  the  Baltimore  and  Ohio  Bailroad,  Cheat  River  grade,  four 
miles  west  from  Rowlesburg,  Preston  County,  West  Virginia. 


BS* 




[See  map,  N n.] 

1.  Sandstone,  massive,  coarse,  yellowish,  Homewood 

C Coal O' 

2.  Coal < Shales,  sandy 

(Coal... O' 

3.  Shales,  brown,  sandy 

4.  Coal,  slaty 

5.  Shales 

6.  Sandstone,  massive 

7.  Sandstone,  flaggy 

8.  Sandstone,  massive,  grayish  white 

9.  Sandstone,  flaggy  

10.  Shales,  brown 

11.  Sandstone,  grayish  white 

12.  Shale,  brown 


' 5") 

' O'A 

' 5 " ) 


Ft.  in. 


Ft.  in. 
60 

6 10 

45 

2 


13.  New  River  coal  beds. 


Coal 

. . O'  5" 

Shale,  gray - 

..  4'  0" 

Coal I 

..  0'  4" 

Shales,  drab,  sandy. . 

..  8'  0" 

Iron  ore 

..  O'  6" 

Shales 

, . 5'  0"  < 

Coal 

..  1'  0"  I 

Shales 

.10'  0"  | 

Coal 

..  0'  4"  I 

Shales,  brown,  sandy. 25'  0" 

Coal 

..  0'  6"  J 

6 J 


3Sf 


14.  Shales,  brown 

15.  Sandstone 

16.  Shales,  buff,  sandy 

17.  Sandstone,  massive,  pebbly 

18.  Concealed,  and  shales 

19.  Top  of  No.  XI,  red  shales. 


Total. 


55  1 


95 


362  5 


Nos.  2 and  4 represent  the  Mercer  coal  group,  Nos. 
fig.  134.— Section  near  ^ ^ the  Connoquenessing  sandstones,  while  No. 

Rowlesburg,  w.  Va.  13  represents  the  New  River  coal  group. 

Section  near  mouth  of  Sandy  Creeh,  Preston  County , West  Virginia. — 
Farther  northwest,  down  Cheat  River,  and  in  the  center  of  the  Ligonier 
basin,  the  Pottsville  series  exhibits  the  following  struc- 
ture (Fig.  135)  near  the  mouth  of  Sandy  Creek,  Preston 
County,  West  Virginia : 

Near  mouth  of  Sandy  Creek,  on  Cheat  River,  Preston  County,  West 

Virginia. 

[See  map,  M m.  J 


Ft. 


1.  Sandstone,  massive,  very  pebbly  near  middle 

2.  Shales,  dark. 


3.  Coal 


( Coal 

O' 

10"  i 

{ Shale 

0' 

3"  > 

( Coal 

0' 

5"$ 

Ft.  in. 
160 
.10 

1 6 


Fig.  135. — Section 
nearmouth  ofSaudy 
Creek,  Preston 
County,  W.  Va. 


4.  Fire  clay 7) 

5.  Slate,  black,  fissile 15  > 37 

6.  Sandstone,  gray 15  ) 

7.  Shale,  with  streak  of  coal  1* 

8.  Sandstone,  grayish  white 15 

9.  Green  and  red  shales  of  No.  XI.  

Total 224  6 

Here,  as  frequently  happens,  the  Mercer  coal  group 
disappears  entirely,  while  the  Homewood  and  Conno- 
quenessing sandstones  unite  into  one  solid  mass.  Nos. 
3 to  7 represent  the  New  River  coal  group. 


WHITE.  J 


THE  POTTSYILLE  CONGLOMERATE. 


189 


Section  on  Booth's  Creek , Taylor  County , West  Virginia,— The  struc- 
ture of  the  Pottsville  beds  in  the  region  along  the  line  between  Taylor 
and  Marion  Counties,  West  Virginia,  is  learned  from  a 
boring  made  for  oil  on  Booth’s  Creek,  Taylor  County,  by 
Mr.  John  L.  Steele,  to  whom  I am  indebted  for  the  fol- 
lowing record  (Fig.  136) : 

Booth's  Creek,  Taylor  County , West  Virginia  (boring). 

[See  map,  O 1.]  Ft. 

1.  Sandstone,  hard,  wliite,  pebbly 159 

2.  Black  slate - . 15 

3.  Shale,  gray  and  sandy 20 

4.  Shale,  black - 15 

5.  Shale,  gray,  sandy . 20 

6.  Sand,  gray,  pebbiy 10 

7.  Bed  beds  of  No.  XI. 


Total 239 

Here  the  structure  is  very  much  like  that  of  the  pre- 
vious section  on  Cheat  River,  and  the  thickness  is  also 
nearly  the  same. 

Section  under  Clarksburg , West  Vir- 
ginia.— Under  Clarksburg,  Harrison 

County,  West  Virginia,  the  succession  is 
given  as  follows  (Fig.  137),  from  the  rec- 
ord of  the  Despard  gas  well,  on  the  authority  of  Prof. 

T.  M.  Jackson: 

Clarksburg,  West  Virginia  (gas  well). 


Fig.  136. — Section 
on  Booth’s  Creek, 
Taylor  County, 
W.  Va. 


[See map,  Ok.] 


1.  Sandstone,  black  — 

2.  Sandstone,  white 

3.  Sandstone,  gray 

4.  Sandstone,  white  — 

5.  Sandstone,  gray 

6.  Sandstone,  dark 

7.  Shale,  black  

8.  Sandstone,  white 

9.  Sandstone,  gray  . — 
10.  Bed  beds  of  No.  XI. 


30  ^ 


Ft. 


174 


Total. 


256 


50' 


U* 


-n> 


i 


Fig.  137. — Section 
under  Clarks- 
burg, W.  Va. 


7 <f 


Section  near  Farmington , West  Vir- 
ginia.— Under  the  central  portion  of 
Marion  County,  West  Virginia,  the 
structure  is  shown  by  the  record  of  the 
HukiH  oil  boring  near  Farmington  (Fig.  138),  as  given 
in  Second  Geological  Survey  of  Pennsylvania,  1886  (pp. 
782,  783) : 

Farmington,  West  Virginia  (oil  boring). 

[See  map,  M 1.] 


Ft. 

1.  Sandstone 100 

10 

17 

70 

12 


Fig.  138. — Section 
near  Farmington, 
W.  Va. 


2.  Shell 

3.  Slate  

4.  Black  slate 

5.  Sandstone 

6.  Bed  beds  of  No.  XI. 


Total 


209 


190 


THE  NORTHERN  BITUMINOUS  COAL  FIELD. 


[BULL.  65. 


Section  under  Wellsburg , West  Virginia. — Under  Wellsburg,  Brooke 
County,  West  Virginia,  the  Barclay  gas  well  No.  1 gives  tlie  following 
(Fig.  139)  for  these  beds  on  the  authority  of  Mr.  Bar- 
clay : 


ijpi 

lllli 


TS!. 


aft' 


14/ 


Wellsburg,  West  Virginia  (gas  boring). 
[See  map,  J j.] 


1.  Sandstone,  white 

2.  Sandstone,  gray  . 

3.  Sandstone,  blue . . 

4.  Coal 

5.  Slate  and  shale. . . 


Total. 


Ft 

75  1 
30  > 

40  j 


Ft. 


145 


31 


182 


ri?-  13^“T,slction  txt"  The  coal  reported  in  this  section  comes  at  the  liori- 

va.  zon  of  the  Sharon  bed  of  Ohio  and  Pennsylvania,  but 

it  was  probably  nearly  all  coaly  slate  or  else  a local  thickening,  since 
other  borings  put  down  in  this  region  do  not  report  it  at  all. 

Section  in  Mercer  County , Pennsylvania. — Along  the  northwestern 
margin  of  the  Appalachian  field  in  the  counties  of  Lawrence  and  Mer- 
cer, bordering  the  Ohio  State  line,  a series  of  workable  coal  beds  make 
their  appearance  in  the  Pottsville  series  and  extend  along  the  margin 
of  the  field  clear  through  to  southern  Ohio.  The  general  section  of  the 
Pottsville  series  of  Mercer  County,  Pennsylvania,  given  in  Q3  ( p.  33), 
Second  Geological  Survey  of  Pennsylvania,  shows  the  succession  of 
these  coal  groups  as  follows  (Fig.  140) : 


Fig.  140 — Section  in 
Mercer  County,  Pa. 


Mercer  County,  Pennsylvania. 
[See  map,  E k.] 


1.  Sandstone,  Homewood 

2.  Shales .... 

3.  Iron  ore 

4.  Limestone,  Mercer,  Upper 

5.  Coal,  Mercer,  Upper 

6.  Shales 

7.  Iron  ore 

8.  Limestone,  Mercer,  Lower 

9.  Shales 

10.  Coal,  Mercer,  Lower 

11.  Shales... 

12.  Iron  ore 

13.  Shales 

14.  Sandstone,  Connoquenessing,  Upper. . 

15.  Shales  with  iron  ore — 

16.  Coal,  Quakertown 

17.  Shales 

18.  Sandstone,  Connoquenessing,  Lower. . 

19.  Shales,  Sharon,  iron  bearing 

20.  Coal,  Sharon .' 

22.  Fire  clay  and  shales 

23.  Sharon  Conglomerate,  base  of  Xo.  XII 

Total 


Ft.  in. 


6 i 

l 


Ft.  in. 
50 


5 

2 

2 6 


44  6 


66 

2 

100 

4 

5 
20 

301 


WHITE.] 


THE  POTTSVILLE  CONGLOMERATE. 


191 


Section  near  Quakertown , Mahoning  County , Ohio . — Where  the  Ohio- 
Pennsylvania  State  line  crosses  the  Mahoning  Eiver,  near  Quakertown, 
these  beds  exhibit  the  following  structure  (Fig.  141) : 


Ohio -Pennsylvania  line  on  Mahoning  River. 

[See  map,  Fk;]  Ft.  in. 


1.  Homewood  sandstone 

2.  Concealed 

3.  Limestone,  Upper  Mercer  . 

4.  Fire  clay 

5.  Sandstone,  shaly 

6.  Coal,  slaty,  Middle  Mercer 

7.  Fire  clay  and  sandy  shales 

8.  Limestone,  Lower  Mercer 

9.  Shales 

10.  Coal,  Mercer,  Lower 

11.  Fireclay 

12.  Shales,  sandy 

13. 

14. 

15. 


Sandstone,  Connoquenessing,  Upper 45 

Coal,  Quakertown 


Fig.  141. — Section  near 
Quakertown,  Ohio. 


Fire  clay  and  shales  . . . 

Qq  ti  f\  atoll p ( ImmnmiP. 

[Sandstone 

- jn 

Oaii'ioiinic,  v/uiiiunpiC’ 

nessing,  Lower 

. ] Sandstone,  flaggy 

...  40' 

[Sandstone,  massive  . - 

...  30', 

3 6 1, 


99 


Blue  shales,  with  iron  ore  halls 20 

Sandstone,  massive 10 

Coal,  Sharon,  and  bituminous  slate 

Sandstone,  flaggy,  to  base  of  No.  XII 

Total 


Ft.  in. 
20 
10 


24  5 


55  6 


1 2 


132  G 


1 6 

25 

270  1 


The  Sharon  coal  of  these  sections  (140,  141)  represents  the  New  Eiver 
coal  group  of  West  Virginia,  since  the  Mercer  group  above  does  not 
furnish  valuable  coal  in  that  region,  but  only  thin  slaty  beds. 

Section  in  Holmes  County , Ohio. — In  Holmes  County,  Ohio,  these  beds 
are  given  as  follows  (Fig.  142),  in  Vol.  V,  Ohio  Geology,  p.  837 : 


Holmes  County , Ohio. 


[See  map,  H e.] 


Fig.  142.— Section 
in  Holmes  Coun- 
ty, Ohio. 


1.  Interval,  sandstone  and  shales 

2.  Limestone,  Lower  Mercer 

3.  Coal,  Lower  Mercer 

4.  Concealed 

5.  Gray  shales 

6.  Coal 

7.  Gray  shale  and  concealed 

8.  Sandstone,  Upper  Connoquenessing 

9.  Coal,  Quakertown 

10.  Sandstone,  shaly,  Lower  Connoquenessing. 

11.  Coal,  thin 

12.  Sandstone 

13.  Coal,  Sharon 

14.  Fire  clay 

15.  Lower  Carboniferous  beds. 


Ft.  in. 
60 

1 G 

17 

6 

2 

23  6 
15  6 
blossom 
33  G 

3 

2 G 
10 


Total 


174  G 


192 


THE  NORTHERN  BITUMINOUS  COAL  FIELD. 


[BULL.  65. 


Section  in  Washington  County , Ohio. — In  Washington  County,  Ohio, 
the  Pottsville  measures  are  given  as  follows  (Fig*  143)  by  Mr.  F.  W. 
Minshall,  from  the  record  of  the  Epler  oil  boring : 

Epler  oil  boring,  Washington  County , Ohio. 

[See  map,  M g.J 


1.  Sandstone 

2.  Shales 

3.  Coal 

4.  Shales 

5.  White,  pebbly  sandstone  .. 

6.  Black  shales 

7.  Lower  Carboniferous  beds. 


Ft. 

24 

20 

70 

60 

4 


Total 178 

Section  at  Parkersburg , West  Virginia. — The  Camden 
Consolidated  Oil  Company,  in  boring  at  Parkersburg, 
fig.  143.— section  West  Virginia,  found  the  following  structure  (Fig.  144), 
CouTtySohfoton  according  to  Mr.  B.  A.  Cole,  the  superintendent: 


Parkersburg , West  Virginia  (boring). 

[See, map,  O f.] 


Ft. 


1.  Shales,  gray 110 

2.  Sandstone,  hard,  white 50 

3.  Slate,  black 25 

4.  Sandstone,  hard,  gray 50 

5.  Shales  of  No  XT. 


Total 


235 


Section  near  Burning  Springs , West  Vir- 
ginia.— Near  Burning  Springs,  Wirt 
County,  West  Virginia,  these  same  beds 
have  this  succession  (Fig.  145),  as  found 
in  the  Simpson  oil  boring  by  Mr.  Min- 
shall : 

Simpson  ivell,  Wirt  County,  West  Virginia. 

[See  map,  P g.] 


Sflf 


50l 


Fig.  144. — Section 
under  Parkers- 
burg, W.  Va. 

Ft. 


Fig.  145.— Section 
near  B u r n in g 
prings,  W.  V a. 


1.  Sandstone 

2.  Coal 

3.  Sandstone 

4.  Shales - 

5.  Coal - 

6.  Sandstone 

7.  Shales 

8.  Sandstone 

9.  Shales 

10.  Coal 

11.  Conglomerate 

12.  Shales  - 

13.  Limestone,  Subcarboniferous. 

Total ,352 

The  Burning  Springs  section  (Fig.  145)  shows  a rapid 
increase  in  the  thickness  of  these  beds  towards  the 
southeast,  since  they  are  just  twice  as  thick  here  as  in 
Washington  County,  Ohio  (Section  143),  .50  miles  distant. 


WHITE.] 


THE  POTTSVILLE  CONGLOMERATE. 


193 


Section  near  Jackson  Furnace , Jackson  County , Ohio. — In  Jackson 
County,  Ohio,  the  Pottsville  series  has  the  following  structure  (Fig. 

146)  near  Jackson  furnace,  as  given  in  the  Ohio  Geo- 
logical Survey,  1870  (p.  158) : 


Jackson  Furnace , Jackson  County , Ohio. 

[See  map,  P b.j 


Ft.  in. 
0 8 
20 

0 7 

15 


1.  Iron  ore  .1 

2.  Interval 

3.  Iron  ore 1 

4.  Coarse  sandstone 

5.  Coal trace 

6.  Shale 18 

7.  Iron  ore 0 6 

8.  Clay,  shale 1 1 

9.  Sandstone,  coarse 20 

10.  Sandy  shales  and  laminated  sandstone 115 

11.  Coal ' . 2 6 

12.  Fireclay  2 6 

13.  Clay,  shale  2 6 

14.  White  sandstone — 10 

15.  Sandy  shale 10 

o'ar  1 - _ 1 n A 


16.  Coal 

17.  Shales  and  sandstones  to  base  of  No.  XII 


Total 238 


fig.  M6.-Section  Section  at  Hanging  Bock , Sciota  County , Ohio. — In  the 
iface^j a^k To ii  vicinity  of  Hanging  Rock,  Ohio,  the  Pottsville  series  has 

County,  Ohio. 


the  following  structure  (Fig.  147) : 


Fig.  147.  — Section 
at  Hanging  Rock, 
Sciota  County, 
Ohio. 


Hanging  Bock , Sciota  County,  Ohio. 


[See  map,  It  a.] 


Ft.  in. 


1.  Sandstone,  massive 

2.  Fire  clay 

3.  Limestone  and  iron  ore,  Upper  Mercer 

4.  Shales  

5.  Coal,  Upper  Mercer 

6.  Fire  clay,  sandy 

7.  Sandstone,  shaly 

8.  Shales,  drab  

( Coal 0'  5 " 1 

9.  Coal,  Lower  Mercer < Fire  clay V 4"  > 

(Coal 1'4") 

10.  Fire  clay  and  shales 

11.  Sandstone,  Connoquenessing,  Upper,  massive,  coarse,  yellowish 

12.  Sandy  shales  and  shaly  sandstone 

( Coal  O'  5"  } 

13.  Coal,  Quakertown < Slate 0'  3''  > 

( Coal V 5") 

14.  Fire  clay 

15.  Sandy  shales 

16.  Sandstone,  Lower  Connoquenessing,  massive 

17.  Shales,  dark  blue,  with  iron  ore 

18.  Iron  ore,  sandy 

19.  Blue  sandy  shales 

20.  Interval  to  base  of  Pottsville  beds  under  river,  from  drill  hole  (E.  B. 

Willard) 


40 

5 

1 

20 

0 

2 

8 

8 


5 

30 

15 


3 

17 

25 

5 

1 

40 

40 


4 


1 


1 


Total 


270  6 


Here  the  Mercer  group,  together  with  the  Quakertown 
coal,  is  distinctly  recognizable  at  the  very  southern  bor- 
der of  Ohio,  while  the  Connoquenessing  sandstones  and 


the  dark  blue  Sharon  iron-bearing  shales  below  look  exactly  like  the 
same  beds  in  eastern  Ohio.  The  base  of  , the  series  was  given  me  here 
from  the  record  of  a bore-hole  put  down  by  Mr.  E.  B.  Willard,  super- 
intendent of  the  Hanging  Rock  Coal  Company. 


Bull  65 13 


194 


THE  NORTHERN'  BITUMINOUS  COAL  FIELD. 


[BULL.  65. 


Section  on  Big  Sandy  River , Lawrence  County,  Kentucky. — Twenty  miles 
up  the  Big  Sandy  River,  and  near  the  mouth  of  Blaine  Creek,  the  suc- 
cession of  the  series  is  as  follows  (Fig.  148)  according  to 
the  record  of  Rigdon  gas  well  No.2,  as  furnished  by  Mr. 
F.  H.  Oliphant: 


€ 


v,\ 


Under  Big  Sandy  River  at  mouth  of  Blaine  Creek  (boring). 
[See  map,  Y b.j 


Ft. 

25 

5 

20 

25 

15 

20 

20 

40 

Sandstone,  white,  salt  water 100 

10 

10 

90 

25 

10 

30 


1.  Sandstone,  white 

2.  Slate,  black 

3.  Sandstone,  white 

4.  Sandstone,  dark  gray. 

5.  Slate,  gray 

6.  Sandstone,  dark 

7.  Slate,  gray 

8.  Sandstone,  dark  gray. 


10.  Sandstone,  dark  blue 

11.  Slate,  black 

12.  Sandstone,  white 

13.  Slate,  black 

14.  Shells 

15.  Sandstone,  hard  blue 

16.  Limestone,  Lower  Carboniferous. 


Total 


445 


This  section  exhibits  the  beginning  of  the  great  south- 
eastern thickening  of  the  Pottsville  series  along  the  Big 
Sandy,  but  we  have  not  sufficient  data  southward  from 
Blaine  Creek  to  trace  the  rate  of  increase  along  the  Tug 
Fork,  since  even  the  top  of  the  Pottsville  does  not  rise 
to  daylight  on  that  stream  for  100  miles  above  the  mouth 
of  Blaine.  When  the  bottom  series  does  finally  come  to 
the  surface  at  the  southern  edge  of  McDowell  County, 
West  Virginia,  it  is  not  less  than  1,500  feet  thick,  and 
may  possibly  be  2,000,  since  the  Kentucky  geologists  claim  the  latter 
thickness  for  these  measures  on  the  headwaters  of  the  Big  Sandy. 

There  is  no  point  along  the  Tug  River  in  West  Virginia  where  a 
vertical  measurement  can  be  made ; hence,  if  the  exact  thickness  is 
ever  determined  it  must  be  by  a boring. 

The  black  slates,  Nos.  2,  11,  and  13  of  the  above  section,  probably 
represent  the  interconglomerate  coal  beds. 


Fig.  148.— Section 
under  Big  Sandy 
Biver  near  mouth 
of  Blaine  Creek. 


WHITE.] 


THE  POTTSVILLE  CONGLOMERATE. 


195 


Section  under  Charleston , Kanawha  County , West  Virginia. — On  the 
Great  Kanawha  River  some  recent  borings  for  gas  have  supplied  the 
necessary  data  there,  thus  giving  measurements  at  two 
points  before  the  whole  formation  comes  to  the  surface. 
The  first  one  of  these  is  the  record  of  the  Edwards  gas 
well  Ko.  3,  bored  at  Charleston,  West  Virginia,  which 
gives  the  following  structure  (Fig.  149)  for  these  beds, 
according  to  Mr.  William  S.  Edwards  : 


^;v;vav 

•/.V.v.y/v.Y.  s 

V- 1 3 

\ \ \ •.  ’.  li 

y.w.v  v/.v.v 

:;’v3r3^Sv 

-1:. d” 

Under  Charleston , Kanawha  County,  West  Virginia  (boring). 
[See  map,  T f.] 

1.  Sandstone 

2.  White  sandstone 

3.  Hard  sandstone  and  shells 

4.  White  sandstone 

5.  Black  sandstone  and  shell 

6.  White  sandstone 

7.  Hard  sandstone 

8.  Hard  black  shells  and  gas 

9.  White  sandstone 

10.  Black  sandstone 

11.  White  sandstone 

12.  Black  sandstone 

13.  White  sandstone 

14.  Hard  shells 

15.  White  sandstone 

16.  Sandsheil,  hard 

17.  White  sandstone 

18.  Black  sand 

19.  Lower  Carboniferous  limestone 


Total 


Ft. 

20 

30 

65 

45 

30 

20 

55 

90 

55 

10 

10 

15 

5 

10 

25 

10 

75 

10 


580 


Here  the  Pottsville  series  has  thickened  to  about  three 
times  its  size  at  the  northwestern  outcrop  of  these  beds 
in  Ohio,  100  miles  distant.  Whether  the  thickening  is 
gradual  or  abrupt  is  not  known,  and  can  not  be  until 
more  borings  are  made.  It  is  probably  gradual  from 
the  center  of  tbe  great  Apalachian  trough,  50  miles 
northwest  of  Charleston. 

The  interconglomerate  coal  beds  appear  to  be  entirely 

^der^cirfries^oS’  al)seut  fr°ra  tlie  a5ove  section,  since  not  even  black 
Kanawha  County’,  slates  are  present  according  to  the  driller’s  record. 


196 


THE  NORTHERN  BITUMINOUS  COAL  FIELD. 


[BULL.  65. 


Section  at  Burning  Spring,  Kanaivha  County , West  Virginia. — At  Burn- 
ing Spring,  9 miles  south  from  Charleston,  the  record  of  Edwards  gas 
well  No.  1 gives  these  beds  as  follows  (Fig.  150) : 


ii® 

w 


$ 176' 


yXvXtfv 

*>> 

VV.V 

Xv.-.v.'.' 

>AVAV.V 

w,v 

^•XVA 

Y/S/.yV. 

;‘vX 

’•.y.v.v 

iv.v-v.X 

.v.'.v.v.v.w. 

f.v.v.’.v.v.v. 

»,*.*-*• vv.v.v; 

Burning  Spring,  Kanawha  County , West  Virginia  (boring). 
[See  map,  Tf.] 


1.  Sandstone,  hard  white 

2.  Coal,  hard 

3.  Sandstone,  hard  white,  salt  water 


6.  Slate,  black 

7.  Sandstone,  hard  white 

8.  Sandstone,  blue  hard 

9.  Limestone,  Lower  Carboniferous 


Ft. 

Ft. 

176 

6 

. 200  . 

* 100  ( 

555 

255  ^ 

2 

50 

50 

. 839 

No.  2 represents  the  Mercer  coal  group,  though  no 
coal  thick  enough  to  mine  ever  occurs’at  this  horizon 
to  the  southward,  where  these  beds  rise  above  water 
level. 

The  New  River  coals  belong  in  Nos.  4 and  6 of  the 
section,  but  they  here  contain  no  coal  whatever,  though 
only  40  miles  north  from  the  New  River  coal  field. 

The  series  has  here  increased  259  feet  in  thickness 
in  9 miles,  a very  rapid  rate,  and  possibly  indicating 
that  the  great  thickness  (580  feet)  found  under  Charles- 
ton may  have  been  abruptly  instead  of  gradually  ac- 
quired. • 

In  this  boring  a considerable  flow  of  natural  gas 
was  obtained  in  the  top  of  the  Pocono  sandstone,  or 
“Big  Injun”  oil  sand,  at  a depth  of  about  1,000  feet. 
This  is  the  locality  where  natural  gas  was  first  used 
for  manufacturing  purposes  in  the  United  States,  as 
far  back  as  1841.  It  was  utilized  for 
evaporating  salt  water.  One  of  the  gas 
wells  found  here,  according  to  report, 
displaced  for  fuel  2,000  bushels  of  coal 
daily  during  a period  of  ten  years.  The 
last  well,  however  (bored  in  1887),  does 
not  produce  much  over  500,000  cubic 
feet  of  gas  daily.  The  most  productive 
wells  were  situated  near  the  crest  of  the 
anticline  which  crosses  the  Kanawha 
River  at  Burning  Spring. 


ITig.  150. — Section  at  Burning  Spring, 
Kanawha  County,  W.  Va. 


WHITE.] 


THE  POTTSVILLE  CONGLOMERATE, 


197 


no' 


17Q4 


IjSff 


Section  near  Nuitallburg , Fayette  County , Virginia . — Passing  on 

southward  up  the  Kanawha  and  New  Rivers,  there  is  no  opportunity 

to  get  another  measurement  of  the 
Pottsville  series  until  all  of  its  mem- 
bers have  risen  above  the  level  of  New 
River,  in  the  vicinity  of  Nuttallburg, 
Payette  County,  W est  Virginia,  50  miles 
distant  from  Burning  Spring,  where 
the  following  succession  occurs  (Fig, 
151): 

Vicinity  of  Nuttallburg , Fayette  County , West 
Virginia. 

[See  map,  U h.] 


. 


I2Q’ 


360" 


4*sT 


aa* 


40' 


<*4% 

IQ 

■arf 


140’ 


420 


Fig. 


151.— Section  in  vicinity  of  Nuttall- 
burg. Fayette  County,  W.  Va. 


2.  Shales 

3.  Coal 

4.  Sandy  shales  and  sandstone  . 

5.  Sandstone 

6.  Black  slate 

7.  Coal 

8.  Shales  and  sandstone 

9.  Coal 

10.  Shales,  sandstone  and  shales. 

11.  Coal,  Nuttall 

12.  Shales  and  slates 


14.  Slates,  dark 

15.  Concealed,  and  shales 

16.  Coal,  Fire  Creek 

17.  Shales  and  sandstone 

( Coal 

I Slate 

18.  Coal,Quinnimont  (?)  •(  Coal 

1 Slate 

Coal 


Ft. 

le-  l 

Ft. 

in. 

170 

..  75) 

1 

" ll 

102 

1 

75 

0 

10 

50 

..  75) 

3 

6 

. . 155  { 

jsJ 

360 

3 

6 

,..  V 0") 
.. . O'  3”  I 
,..  2'  0" 
...O'  2"  \ 
...  r 0" J 

130 

4 

5 

420 


19.  Shales  and  sandstone 

20.  Coal,  slaty 

21.  Shales 

22.  Coal 

23.  Shales 10  ] 

24.  Concealed  30 

25.  Sandstone,  mastive 125  | 

26.  Concealed,  and  sandstone 60 

27.  Sandstone,  massive  140  1 

28.  Concealed,  and  sandstone  to  top  of 

No.  XI  shales „...  55  J 


Total 1,400  0 

No.  11,  the  Nuttall  coal,  is  the  highest 
member  of  the  New  River  group  that 
ever  furnishes  valuable  coal  along  that 
stream.  Its  place  in  the  Pottsville 
series  is  400  feet  below  the  top,  and  the 
other  thin  coals  above  it  belong  to  the 
Mercer  group. 

Whether  No.  18  is  identical  with  the 
Quinnimont,or  whether  this  latter  coal 
is  the  same  as  the  Fire  Creek,  No.  16, 
are  questions  yet  unsettled. 

Just  what  represents  the  Pocahontas 
coal  of  McDowell  and  Mercer  Counties 
in  this  section,  or  whether  it  is  repre- 


sented at  all  is  uncertain,  but  No.  IS  may  possibly  come  at  that  horizon. 


198 


THE  NORTHERN  BITUMINOUS  COAL  FIELD. 


[DULL.  65. 


Section  on  Crane  Creelc,  Mercer  County,  West  Virginia. — At  the  ex- 
treme southern  edge  of  the  Appalachian  field  in  Mercer  County,  West 


Fig.  152. —Section  on  Crane  Creek,  Mercer 
County,  W.  Ya. 


Virginia,  the  following  section  (Fig.  152) 
of  the  Pottsville  series  was  obtained 
upon  the  waters  of  Crane  Creek  by  add- 
ing 400  feet  to  the  summit  of  the  column 
for  the  estimated  thickness  of  beds  re- 
moved by  erosion : 

Crane  Creek,  Mercer  County,  West  Virginia. 

[See  map,  Y g.  ] Ft.  Ft.  in. 


1.  Sandstones  and  shales,  here  eroded  from 

top  of  No.  XII  (estimated) 

2.  Shales  and  sandstones 

3.  Sandstone  and  shales 

4.  Sandstone,  gray 

5.  Shales,  and  concealed 

6.  Sandstone,  massive,  and  shales. 


7.  Coal i 


Coal 

0'  2"  | 

Shales 

....  2'  6"  1 

Coal 

...  2'  4"  ; 

Shale 

....  O'  6"  i 

Coal 

....  1'  8"  I 

Shales,  sandstone,  and  concealed. 

Shales 

Coal,  good  

Shales,  and  concealed 

Sandstone 

Shale 

Coal . 

Coal <(  Shale 

Coal  and  slate. 

Concealed,  with  shales,  sandstones,  and 
two  thin  coals 

( Coal 2'  6" 

< Shale; 5'  0" 

( Coal 6'  0" 


Coal.  Pocahontas 
(No.  Ill) 


17.  Shales,  sandstone,  and  concealed 

18.  Coal  (No.  II) 

19.  Sandstone  and  shales 

20.  Coal  (No. I)  

21.  Shales 

22.  Sandstone,  gray 

23.  Shales,  dark 

24.  Concealed 

25.  Sandstone,  and  concealed 

26.  Sandstone,  gray,  massive 

27.  Green,  limy,  fossiliferous  shales,  top  of 

Lower  Carboniferous. 


4001 

1U0  | 

35 
20  f 

60  I 

95  J 


110  / 

55 

100) 

10  ? 

3) 


28) 
35 
20  ( 
50  f 
40  | 
10  J 


710 


7 2 

115 
1 8 

113 

6 

130 

13  6 

80 
2 6 
20 
0 2 

183 


Total 1,402 

The  interval  added  to  the  top  of  the 
Pottsville  in  this  section  is  only  an  esti- 
mate at  best,  and  the  amount  may  not 
be  near  large  enough,  since  the  Ken- 
tucky geologists  report  the  series  as 
2,000  feet  thick  not  many  miles  south- 
west from  this  region. 

The  separate  coal  beds  of  this  section 
can  not  yet  be  satisfactorily  correlated 
with  those  on  New  River  (Section  151); 
At  one  time  the  writer  was  inclined  to 
believe  that  No.  7 might  be  the  equiva- 
lent of  the  Nuttall  vein,  and  that  No.  16 
of  this  section  was  probably  identical 
with  No.  18  of  the  Nuttallburg  section 


WHITE.] 


THE  HOMEWOOD  SANDSTONE. 


199 


(151),  but  the  Pocahontas  coal  lies  200  feet  nearer  the  base  of  the 
Pottsville  series  than  No.  18  does  on  New  River,  and  hence  unless  this 
part  of  the  series  thins  away  towards  the  southwest,  which  seems  im- 
probable, the  possibility  of  identity  is  rather  slender.  The  miuing 
operations  of  the  next  few  years,  however,  may  be  depended  upon  to 
settle  the  question,  since  it  has  a more  than  scientific  interest. 

A cursory  examination  of  the  sections  given  will  show  that  the 
Pottsville  series  generally  has  something  like  the  following  structure : 

Sandstone  (Homewood). 

Coal  group  (Mercer). 

Sandstones  (Counoquenessing). 

Coal  group  (New  River). 

Sandstone  (Sharon). 

Of  course  when  the  series  attains  such  an  excessive  thickness  as  on 
the  New  River,  for  instance,  the  structure  is  more  complicated  than  the 
above  scheme  would  indicate,  and  yet  even  then  a general  agreement 
can  usually  be  made  out. 

Having  now  glanced  at  the  general  structure  of  these  measures,  we 
shall  take  up  the  more  important  members  and  describe  them  in  detail. 

CHARACTERISTIC  HORIZONS. 

THE  HOMEWOOD  SANDSTONE. 

The  Pottsville  series  is  nearly  everywhere  capped  with  a coarse 
sandstone,  which  is  quite  different  in  texture  and  general  appearance 
from  any  of  the  sandstones  in  the  Coal  Measures  above.  In  the  vicinity 
of  Homewood,  Beaver  County,  Pennsylvania,  this  rock  attains  a thick- 
ness of  150  feet,  and  was  named  from  that  locality.  It  is  generally 
quite  massive,  making  great  cliffs  along  the  streams  and  covering  the 
summits  with  huge  blocks  arranged  in  “rock  cities.”  While  usually 
quite  hard,  it  generally  splits  well  and  makes  excellent  building  stone, 
the  blocks  from  it  being  almost  indestructible.  Although  generally  of 
a yellowish  or  buffish  gray  tinge,  it  occasionally  consists  of  almost  pure 
white  quartz  grains,  and  hence  sometimes  supplies  glass  sand  of  excel- 
lent quality.  This  might  be  called  the  “ cascade”  member  of  the  Potts- 
ville series,  since  it  so  often  produces  water-falls. 

In  Pennsylvania  it  is  generally  30  to  50  feet  thick,  but  occasionally, 
as  at  Homewood  and  other  points,  it  thickens  up  to  75  or  even  150  feet. 

Westward,  in  Ohio,  the  rock  thins  down  and  is  often  only  15  to  20 
feet  thick,  but  still  distinctly  recognizable  as  a heavy  bedded,  coarse 
sandstone,  filled  with  fossil  stems  and  trunks  of  trees,  mostly  lepido- 
dendron  and  sigillaria.  It  is  seen  in  the  bed  of  Little  Beaver  near  its 
mouth,  and  frequently  between  that  point  and  Fredericktown.  It  is 
the  quarry  rock  in  Coshocton  County  referred  to  in  Vol.  V (p.  104),  Ohio 
Geology,  where  it  is  30  feet  thick  and  of  the  same  type  so  often  found 
in  Pennsylvania.  From  this  point  on  across  Ohio,  to  Irouton  and 


200 


THE  NORTHERN  BITUMINOUS  COAL  FIELD. 


[BULL.  65. 


Hanging  Rock,  it  is  frequently  seen,  and  at  the  latter  point  makes  one 
of  the  great  cliffs  in  the  steep  hillside  which  gave  name  to  the  place, 
being  there  40  feet  thick. 

Along  the  Great  Kanawha  this  rock  comes  to  water  level  at  the 
mouth  of  Armstrong  Creek,  and  from  there  on  up  that  stream,  as  well 
as  up  the  New  and  Gauley  rivers,  is  a great  cliff  rock  150  to  200  feet 
thick.  It  crowns  the  walls  of  the  New  River  canon  at  Hawk’s  Nest 
and  other  points  to  Nuttallburg  and  beyond,  where  it  seems  to  change 
suddenly  in  character  southward  from  that,  becoming  soft  and  easily 
disintegrating  to  a heap  of  coarse,  brown  sand. 

On  the  Tug  fork  of  Big  Sandy  this  stratum  makes  great  cliffs  along 
the  hills  through  the  “roughs”  of  Tug,  and  sinks  below  that  stream  at 
the  mouth  of  Ben’s  Creek,  95  miles  above  Louisa. 

Ohio  Pyle  Falls,  on  the  Youghiogheny  River,  is  made  by  this  rock, 
and  the  upper  portions  of  the  great  cascades  on  the  Black  Water  and 
Glady  forks  of  Cheat  pour  over  the  same  stratum. 

It  is  the  gas-bearing  member  in  western  Pennsylvania  and  northern 
West  Virginia. 

THE  MERCER  GROUP. 

In  western  Pennsylvania  a group  of  coals  associated  with  two  fossil- 
iferous  limestones  makes  its  appearance  directly  under  the  Homewood 
sandstone,  and  extends  almost  uninterruptedly  across  the  Ohio  field  to 
Hanging  Rock.  It  was  first  fully  described  from  the  vicinity  of  Mercer, 
Pennsylvania,  and  named  from  that  locality.  When  well  developed 
the  group  presents  the  succession  seen  in  Section  140,  and  is  40  to  50 
feet  thick. 

The  two  limestones  are  very  much  alike,  except  the  Lower  Mercer  is 
a little  darker  blue  than  the  Upper,  and  is  the  more  persistent.  Both 
are  crowded  with  fossils  and  are  frequently  cherty,  some  of  the  famous 
“ flint  ledges  ” of  Ohio  being  made  by  one  of  these  beds.  Each  lime- 
stone usually  carries  an  iron  ore  on  its  top  of  the  variety  known  as 
“block”  ore.  The  Upper  Mercer  is  known  as  the  Zoar  limestone  in 
many  portions  of  Ohio,  and  its  ore  is  called  by  several  terms,  among 
which  are  u Dunkel  Block,”  “Franklin  Block,”  “Main  Block,”  “Big 
Red  Block,”  etc.  The  Lower  Mercer  was  formerly  known  as  the  “Blue' 
limestone,  and  its  corresponding  ore  as  the  “Blue  Limestone  Block,” 
“ Little  Block,”  etc. 

The  Mercer  coals  are  generally  two,  the  upper  one  coming  under  the 
Upper  Mercer  limestone  and  the  lower  one  under  the  Lower  Mercer 
limestone.  Occasionally  there  is  also  a coal  on  top  of  each  limestone, 
but  these  beds  are  sporadic,  and  hence  do  not  merit  a designation, 
though  Orton  has  applied  the  name  “ Tionesta”  to  the  Upper  one  in 
Ohio,  as  the  writer  did  in  Report  Q2,  on  Lawrence  County,  Pennsyl- 
vania. 

These  Mercer  coals  are  generally  rich  in  ash,  and  are  seldom  mined 
on  a commercial  scale,  although  they  are  quite  persistent  from  western 


WHITE.  | 


THE  CONNOQUENESSING  SANDSTONES. 


201 


Pennsylvania  all  around  the  northern  margin  of  the  Ohio  coal  field. 
Both  of  them  occasionally  become  cannel  in  Ohio,  the  upper  being  the 
Strawbridge  cannel  of  Holmes  County  and  the  Bedford  cannel  of  Co- 
shocton, according  to  Orton,  while  the  lower  coal  is  the  Flint  Bidge 
cannel  of  Licking  County.  Neither  of  these  beds  seldom  exceeds  3 feet 
in  thickness,  and  they  are  more  frequently  only  1 or  2. 

Eastward  from  Mercer  and  Lawrence  Counties,  Pennsylvania,  the 
limestones  disappear  from  this  group  and  the  coals  thin  away,  except 
around  the  northern  rim  of  the  coal  field,  where,  in  McKean  County, 
the  Alton  coal  group  of  Ashburner  probably  represents  the  Mercer 
coals,  so  that  usually  only  one  is  left,  and  it  is  generally  quite  impure. 
This  bed  has  received  a different  name  for  nearly  every  locality  where 
it  attains  workable  thickness.  Bogers  called  it  the  Tionesta  coal  in 
Forest  County,  Pennsylvania,  and  it  is  the  Mount  Savage  bed  of  Som- 
erset. Along  the  north  Potomac  Biver  it  frequently  appears  in  the 
cuts  of  the  West  Virginia  Central  Bailroad,  and  is  there  known  as  the 
“Bailroad  seam.”  It  has  been  mined  for  local  use  just  above  Valley- 
Falls,  Taylor  County,  West  Virginia,  where  it  lies  near  water  level, 
and  is  4 feet  thick,  with  a slate  near  center.  It  always  presents  a coarse 
structure,  and  no  first-class  fuel  is  ever  obtained  at  this  horizon.  Along 
the  New  Biver,  and  through  ail  the  country  between  it  and  the  Tug 
Fork,  only  an  insignificant  coal,  1 to  2 feet  thick,  occurs  at  this  level. 

The  famous  Mount  Savage  fire  clay  of  Pennsylvania  and  Maryland 
comes  within  the  limits  of  the  Mercer  group,  and  directly  underlies  the 
Mount  Savage  coal,  which  it  occasionally  replaces. 

THE  CONNOQUENESSING  SANDSTONES. 

Below  the  Mercer  group-  there  comes  the  great  sandstone  horizon 
par  excellence  of  the  Pottsville  series.  This  group  is  generally  triple, 
there  being  a massive  sandstone  at  top,  then  a coal  and  shale  interval, 
below  which  is  another  massive  sandstone.  These  sandstones  were 
first  studied  by  the  writer  along  the  Oonnoquenessiug  Biver,  in  Law- 
rence County,  Pennsylvania,  and  they  were  designated  from  that 
stream.  The  Massillon  sandstone  of  Newberry  represents  only  a por- 
tion of  the  group;  otherwise  it  would  have  precedence  in  nomenclature. 

Each  of  these  sandstone  members  is  from  40  to  50  feet  thick,  though 
occasionally  the  shale  and  coal  separating  them  thins  out  and  they 
coalesce  into  one  mass  150  to  200  feet  thick,  or  even  more.  They  are 
generally  quite  hard,  the  quartz  grains  being  finer  and  more  compactly 
arranged  than  in  the  Homewood  sandstone  above.  The  color  is  more 
frequently  yellowish  white  than  any  other,  though  sometimes  it  is  gray. 

The  Quakertown  coal  comes  between  the  two  sandstone  members  of 
the  group.  It  seldom  exceeds  2 feet  in  western  Pennsylvania  or  east- 
ern Ohio,  and  unless  it  should  be  the  “ Jackson  shaft,”  or  u Wellstou” 
coal,  it  does  not  seem  to  attain  much  importance  in  that  State,  though 
it  is  often  present  in  the  series  as  a thin  bed,  being  represented  in  the 


202  THE  NORTHERN  BITUMINOUS  COAL  FIELD.  [bull.  65. 

Hanging  Rock  section  (147)  by  number  13,  which  is  only  2 feet  thick, 
slate  and  all.  . 

East  from  the  Mahoning  River  no  workable  coal  is  known  at  this 
horizon  in  Pennsylvania,  though  a thin  coal  or  black  slate  is  often 
present. 

THE  NEW  RIVER  COAL  GROUP. 

The  great  development  of  coal  in  the  middle  and  lower  half  of  the 
Pottsville  series  along  New  River,  West  Virginia,  has  given  name  to 
this  group.  Although  there  are  thin  representatives  of  the  group  in 
nearly  every  section  of  the  Pottsville  which  is  exposed  in  Pennsylvania, 
yet  only  around  the  northwestern  margin  of  the  field  in  that  State  is 
any  valuable  coal  found  at  this  horizon,  namely,  the  Sharon  coal  of 
Mercer  County.  This  bed  occurs  in  pockets  and  isolated  basins,  in  the 
western  part  of  Mercer,  where  it  is  3 to  5 feet  thick,  and  a “ block,”  or 
open-burning  coal  of  great  purity.  It  enters  Ohio  in  the  same  patchy 
condition,  and  extends  through  Mahoning,  Trumbull,  Portage,  Summit, 
Stark,  Medina,  and  Wayne  Counties  of  northeastern  Ohio,  and  it  is 
probably  the  “Jackson  shaft”  or  “ Wellston”  seam  of  Jackson  County 
in  southern  Ohio.  In  all  cases  it  is  the  same  open-burning,  pure  fuel, 
very  low  in  ash  and  sulphur. 

This  Sharon  bed  and  its  thin  rider  appear  to  represent  all  the  coals 
iu  the  New  River  group,  and  hence  it  can  not  be  called  identical  with 
any  one  of  them,  though  according  to  Prof.  Fontaine  the  flora  of  the 
Sharon  roof  shales  is  very  similar  to  that  found  in  the  roof  of  the 
Quinnimont  bed  on  New  River.  These  roof  shales  of  the  Sharon  coal 
through  western  Pennsylvania  and  across  Ohio  are  a very  character- 
istic feature.  They  begin  directly  under  the  Connoquenessing  sand- 
stones, and  are  often  40  to  50  feet  thick;  of  a dark  blue  color,  and 
generally  contain  much  iron  ore  (carbonate)  in  nuggets  and  bands. 
These  shales  show  the  same  character  at  Hanging  Rock  (Section  147), 
in  southern  Ohio,  as  they  do  on  the  Mahoning  at  the  east. 

In  passing  southward  from  Pennsylvania,  along  the  Alleghany  Moun- 
tain region,  one  of  these  New  River  beds  thickens  up  to  3 feet  in  Garrett 
County,  Maryland,  just  east  from  the  West  Virginia  line,  and  has  there 
been  mined  for  local  use  on  the  land  of  Mr.  Browning.  It  comes  near 
the  base  of  the  Pottsville  series,  is  quite  soft  and  pure,  and  exhibits  the 
same  coking  type  as  these  coals  all  do  on  New  River.  One  of  these 
beds  is  also  workable  along  Shaver’s  Fork  of  Cheat  River,  east  from 
the  Beverly  Valley.  This  coal  group,  which  is  well  shown  in  the  Black 
Water  section  (133)  of  Tucker  County,  grows  in  importance  southwest- 
ward  through  Randolph,  Webster,  Greenbrier  and  Nicholas  Counties, 
into  Fayette,  where  at  Nuttallburg  on  New  River  we  find  the  type 
section  of  the  group  (No.  151),  which  there  incloses  three  workable  coal 
beds  besides  several  too  thin  to  be  of  economic  importance.  The  three 
workable  beds  are,  in  descending  order,  the  Nuttall,  Fire  Creek,  and 
Quinnimont,  with  the  intervals  separating  them  shown  in  Section  151. 


THE  POTTSVILLE  CONGLOMERATE  CLIFFS  AND  DEBRIS  ON  NEW  RIVER,  WEST  VIRGINIA,  NEAR  FAYETTE. 


THE  LIBRARY 
OF  THE 

UNIVERSITY  OF  ILLINOIS 


WHITE.] 


THE  NEW  RIVER  COAL  GROUP. 


203 


These  coals  vary  from  3 to  5 feet  in  thickness  along  New  River,  and 
are  the  ones  from  which  the  celebrated  New  River  coke  is  now  manu- 
factured. The  Nut  tall  is  the  most  regular  and  persistent,  being  th£ 
only  one  which  dips  below  water  level  at  the  north  with  a workable 
thickness. 

They  are  all  quite  soft,  very  low  in  ash  and  sulphur,  and  rich  in  fixed 
carbon,  making  coke  of  the  greatest  purity. 

The  Fire  Creek  and  Quinnimont  beds  are  quite  irregular  in  their  dis- 
tribution and  thickness,  but  both  of  them  furnish  much  good  coal  on 
New  River.  I have  termed  the  lowest  bed  the  Quinnimont,  but  the 
stratigraphical  horizon  of  the  Quiunimont  seam  is  not  yet  settled-  since 
it  may  prove  identical  with  the  Fire  Creek  bed,  but  all  the  coal  oper- 
ators agree  that  there  are  three  workable  coals  on  New  River,  and  that 
Nos.  11,  16,  and  18  of  Section  151  are  these  three  beds,  whatever  their 
identity  with  reference  to  the  Fire  Creek  and  Quinnimont  localities 
may  be. 

South  westward  from  Fayette  County  towards  Raleigh,  Mercer,  and 
McDowell,  the  New  River  coals  still  continue  to  increase  in  thickness 
and  importance,  culminating  in  the  great  bed  at  Pocahontas,  in  the  edge 
of  Virginia. 

Section  on  Crane  Creek , West  Virginia , near  Pocahontas , Virginia. — 
Section  152  shows  the  succession  of  these  coals  on  Crane  Creek,  a trib- 
utary of  Blue  Stone,  a few  miles  northeast  from  Pocahontas.  Here 
the  Pocahontas  coal  is  divided  into  two  benches  by  a layer  of  shale  5 
feet  thick,  but  at  Pocahontas  it  exhibits  the  following  structure: 

Ft.  in. 

Coal 9 6 ] Ft.  in. 

Shale 0 4 )>  g 

Coal 0 10  j 


There  is  a bony  streak  about  2 feet  below  the  top  of  the  coal,  but  it 
is  not  rejected  in  mining. 

Section  at  head  of  South  Elk  Horn  Creek , McDowell  County,  West  Vir- 
ginia.— Across  the  Flat  Top  Mountain  divide  from  Pocahontas,  around 
the  head  of  South  Elk  Horn  Creek,  in  McDowell  County,  this  coal  ex- 
hibits the  following  structure: 

Ft.  in. 

Coal 3 8 ') 

Bony  coal 0 8 I Ft. 

Coal 2 3 )>  9 

Coal 2 4 J 


Section  on  East  Branch  of  Simmons  Creek , Mercer  County,  West  Vir- 
ginia.— On  the  east  branch  of  Simmons  Creek  this  coal  shows  as  follows: 


Coal 

Slate,  blue 
Coal 


Ft. 

2 

0 

0 


in. 

2 ) Ft.  in. 

4 ) 8 10 


204 


THE  NORTHERN  BITUMINOUS  COAL  FIELD. 


[BULL.  65. 


Section  on  west  branch  of  Flipping  Creelc , Mercer  County , WestVirginia. — 
On  the  Walker  tract,  west  branch  of  Flipping  Creek,  the  coal  has  this 
structure : 


Ft.  in. 


Coal 

Dark  shales 
Coal 


2 

10 

6 


6 

0 

0 


) Ft.  in. 
>18  6 


Section  on  Pinnacle  Fork  of  the  Guyandotte  River,  Wyoming  County , 
West  Virginia. — Just  before  this  coal  passes  under  the  level  of  the 
Pinnacle  Fork  of  the  Guyandotte  Eiver  west  from  Flat  Top  Mountain 
it  exhibits  the  following  structure : 

Ft.  in. 


Massive  sandstone 

Coal 

Fire  clay 

Sandy  shale 

Coal 


1 

3 


5 

5 


4 

0 

0 

4 


Ft.  in. 
14  8 


This  coal  was  numbered  III  in  the  original  section  published  from 
Pocahontas  by  Maj.  Jed.  Hotchkiss,  and  it  is  frequently  known  by  that 
name.  Major  Hotchkiss  thinks  the  Pocahontas  bed  identical  with  the 
Quinnimont  of  New  Kiver,  but  the  writer  can  not  yet  satisfactorily  cor- 
relate this  bed  with  any  of  the  New  River  coals  which  have  been  mined. 

The  coal  from  the  Pocahontas  seam  is  quite  as  pure  and  valuable  for 
coke  and  general  fuel  purposes  as  any  in  the  New  River  field,  and,  in 
fact,  is  the  same  kind  of  coal. 

Two  other  beds  of  4 to  5 feet  in  thickness  occur  in  the  hills  above  the 
Pocahontas  vein,  but  so  far  they  have  not  been  mined  to  any  extent,  as 
they  are  not  regular  in  thickness  and  the  great  bed  below  monopolizes 
the  present  mining  operations. 


THE  SHARON  CONGLOMERATE. 

The  interval  below  the  Sharon  coal  in  Ohio  and  western  Pennsylvania 
down  to  the  base  of  the  Pottsville  series  is  often  occupied  by  a mass- 
ive conglomerate,  and  when  it  is  absent  the  coal  with  its  under-clay 
rests  directly  on  the  Lower  Carboniferous  beds.  This  conglomerate 
stratum  was  considered  a separate  member  of  the  series  by  the  Ohio 
geologists  and  as  representing  the  entire  No.  XII  conglomerate  of  Rog- 
ers in  Pennsylvania. 

But  later  studies  have  shown  that  it  is  simply  the  basal  member  of 
this  series.  When  well  developed  in  Ohio  it  is  very  coarse,  being  a 
mere  mass  of  pebbles  from  a pea  to  an  egg  in  size.  There  is  no  single 
stratum  around  the  southeastern  margin  of  the  Appalachian  field  that 
will  exactly  compare  with  the  Sharon  conglomerate  in  physical  aspect, 
though  local  streaks  in  all  these  great  sandstones  are  quite  as  pebbly, 
but  just  as  the  Sharon  coal  is  represented  by  several  beds  in  the  New 
River  section,  so  the  Sharon  conglomerate,  only  20  to  40  feet  thick  in 


WHITE.] 


THE  LOWER  CARBONIFEROUS. 


205 


Pennsylvania  and  Ohio,  is  on  New  Biver  represented  by  300  to  400  feet 
of  shales,  sandstones,  and  conglomerates. 

In  northern  Pennsylvania  the  Olean  con  glomerate  of  Bradford  County 
and  the  Garland  conglomerate  of  Warren  have  been  shown  by  Mr.  John 
F.  Carll  to  be  identical  with  the  Sharon  stratum,  and  they  also  resemble 
it  very  much  in  physical  characters.  The  coarse  type  of  the  Sharon 
conglomerate  appears  to  be  confined  to  the  northwestern  rim  of  the 
Appalachian  field,  since  it  disappears  southward  under  the  other  mem- 
bers of  the  series. 

the  lower  carboniferous  beds. 

Below  the  base  of  the  Pottsville  series  come  the  red  shales  and  lime- 
stones of  the  Mauch  Chunk  series,  and  then  succeed  the  gray  sandstones 
of  the  Pocono,  the  lowest  series  of  the  Carboniferous  system. 

Thin  coals  occur  locally  in  both  of  these  members  of  the  Lower  Car- 
boniferous in  Pennsylvania  and  West  Virginia,  but  nowhere  in  these 
States,  nor  in  Ohio,  does  any  merchantable  bituminous  coal  exist  in 
this  portion  of  the  Carboniferous. 

The  Tipton  Bun  coals  of  Blair  County,  Pennsylvania,  have  been  cited 
as  occurring  in  the  Pocono  sandstone  series  for  the  last  thirty-five  years, 
and  this  conclusion  is  reiterated  by  Mr.  Ashburner  in  a special  report 
made  as  late  as  1885  (Pennsylvania  Geological  Survey,  Annual  Beport, 
1885,  p.  250),  but  a single  glance  at  the  fossil  plants  occurring  in  the 
roof  shales  of  the  coals  now  mined  there  proves  that  they  belong  to  the 
Lower  Coal  Measures,  or  Alleghany  Biver  series,  and  not  to  the  Pocono, 
their  apparent  stratigraphical  position  being  the  result  of  displacement, 
so  that  although  the  Pocono  series  is  reported  to  contain  valuable  coal 
beds  in  Montgomery  County,  Virginia,  it  certainly  does  not  in  any  of 
the  three  States  covered  by  this  report,  and  hence  a further  consider- 
ation of  the  Lower  Carboniferous  beds  is  not  germane  to  this  publica- 
tion. 


INDEX. 


A. 

Page. 

Aleppo  Township,  Greene  County,  Penn- 
sylvania, section  in — 24 

Alleghany  County,  Maryland,  section 

in 56 

Alleghany  County,  Pennsylvania,  sections 

in 73,112 


Alleghany  River  series 99-178 

table  showing  strata  of 101 

Alton  coal  group = Mercer  coals 201 

Ames  limestone 90-91 

Andrews,  E.  B.,  section  given  by 28 

Antiquity,  Ohio,  section  at 53 

Arbuckle,  West  Virginia,  section  at 54 

Armstrong  County,  Pennsylvania,  sec- 
tions in 107, 108, 109, 110,  111,  184 

Armstrong  Creek,  West  Virginia,  section 

at  mouth  of 140 

Arno  coal 167 

Ashlmnier,  C.  A.,  sections  given  by 104, 182 

geologi  c identifications  by 174 

Athens  County,  Ohio,  sections  in 66, 133, 134 

B. 

Baird  Ore,  Ohio 173 

Bakerstown  coal 92-93 

Baltimore  and  Ohio  Railroad,  section  on. . 188 

Barbour  County,  West  Virginia,  sections 

in 128,161 

Barclay,  Mr.,  section  furnished  by 190 

Baresville,  Ohio,  section  at 28 

Barnet  coal=  Middle  Kittanning  coal 166 

Barren  Measures  or  Elk  River  series  ...  19,  70-98 
Beaver  County,  Pennsylvania,  section  in.  112 
Beaver  River,  Pennsylvania,  section  near 

mouth  of 172 

Beaver  Run,  Pennsylvania,  section  on...  114 

Bedford  County,  Pennsylvania,  sections 

in  77,149 

Bellaire,  Ohio,  section  at 68 

section  near 50 

Bellton,  West  Virginia,  section  at 26 

Bellton  coal  group 32,  34 

Belmont  County,  Ohio,  sections  in 50,  67,  68 

Bennington,  Pennsylvania,  section  at 122 

Ben's  Creek,  Cambria  County,  Pennsylva- 
nia, section  at 120 

Berlin,  Pennsylvania,  section  at 76 

Berry’s  Mine,  Morgan  County,  Ohio,  sec- 
tion at 67 

Big  Hurricane  Creek,  Putnam  County, 

West  Virginia,  section  at 55 


Tfege. 


Big  Sandy  River,  Lawrence  County,  Ken- 
tucky, section  on 194 

Black  Fossiliferous  limestone 93 

Blacksville  limestone 36 

Blaine  Creek,  Lawrence  County,  Ken- 
tucky, section  at  mouth  oi 144 

section  on 162-163 

Blair  County, Pennsylvania,  section  in...  122 

Blossburg,  Pennsylvania,  section  at 102 

Bloss  vein,  Pennsylvania= Lower  T4ittan- 

ning  c^al 169 

Board  Tree  Tunnel,  Marshall  County, 

West  Virginia,  section  at 25 

Bolivar  fire  clay 159-160 

Bolivar,  Pennsylvania,  section  near 115 

Booth’s  Creek,  West  Virginia,  section  on.  189 

Brady  Township,  Butler  County,  Pennsyl- 
vania, section  at 107 

Broad  Top,  Pennsylvania,  section  at 76-77 

Broad  Top  Basin,  Huntingdon  County, 

Pennsylvania,  sections  in 125, 126, 185 

Brockway ville,  Pennsylvania,  section  near  104 

Brooke  County,  West  Virginia,  section  in  190 

Brookville,  Pennsylvania,  section  at 183 

Brookville  coal=Clarion  coal  in  Ohio  ....  175 

Brookville  coal 178 

Brown,  C.  N.,  sections  furnished  by 50,  67,  68 

Brown’s  Mills,  Monongalia  County,  West 

Virginia,  section  near 38 

Brownstown,  West  Virginia,  section  near  189 

Brownsville,  Pennsylvania,  section  at 44 

Brownsville  coal=Washington  coal 37 

Browntown  sandstone 58 

Brush  Creek  coal  = Masontown  coal 94,  96 

Brush  Creek  coal  = Mahoning  coal 96 

Brush  Creek  limestone  = Lower  Cam- 
bridge limestone 93 

Bryan’s  Bank,  Upshur  County,  West  Vir- 
ginia, section  at 152 

Buckbannon  River,  West  Virginia,  section 

on 152 

Bnchtel  limestone  = Upper  Freeport 159 

, Bnchtel,  Ohio,  section  near 133 

Buffalo  Creek,  Marion  county,  West  Vir- 
ginia, section  at 48 

Buhrstone  iron  ore 173 

Burning  Spring,  Kanawha  County,  West 

Virginia,  natural  gas  first  used  at.  196 

section  at 196 

Burning  Springs,  Wirt  County,  West  Vir- 
ginia, sections  at 52,  83 

section  near 192 

Butler  County,  Pennsylvania,  section  in . . 107 

207 


208 


INDEX. 


Cabell  County,  West  Virginia,  sections 

in . .,..66, 

Cambridge  limestones 

Cambria  County,  Pennsylvania,  sections 

in .118, 119, 120, 122, 

Campbell’s  Creek  coal  vein 

Campbell’s  Creek  limestone 

Camp  Branch,  Cabell  County,  West  Vir- 
ginia, section  near 

Cannelton  coals 

Cannonsburg,  Pennsylvania,  section  at.. . 
Carboniferous  System,  Rogers’s  table 

showing  subdivisions 

Carll,  John  F.,  geologic  identifications  by. 
Carpenter’s  station,  Pennsylvania,  section 

near 

Cassville  plant  shale 

Cedar  Grove  coal 

Centreville,  Pennsylvania,  section  near... 
Chance,  H.  Martyn,  sections  given  by . . . 

107, 

cited  on  geologic  equivalent  of  Upper 

Kittanning  in  Pennsylvania 

geologic  identifications  by 

Chapline  Hill,  Wheeling,  West  Virginia, 

section  at 

Charleston,  West  Virginia,  section  near. . . 

sections  at 

Cheat  River,  Tucker  County,  West  Vir- 
ginia, sections  on 

Clarion  coal 

Clarion  County,  Pennsylvania,  sections 


Page. 

155, 158 
93 

148, 149 
170 
168 

155 

97 

78 

19 

205 

113 
41 
167 
108 
105, 106, 
123, 183 

165 
175, 178 


85 

136, 195 


187, 188 
175-176 


in 105, 106, 183 

Clarion  sandstone 176 

Clarksburg  limestone 88 


Clarksburg,  West  Virginia,  sections  at.. 48-49, 129, 

189 


coal  bed  at 88 

Clearfield  County,  Pennsylvania,  sections 

in 103, 124, 182 

Clearfield,  Pennsylvania,  sections  at. . .123, 182-183 
Clinton  coal  = Middle  Kittanning  coal...  166 
Coalburg,  West  Virginia,  coal  beds  at ... . 96 

section  at 162 

Coal  Valley  gas  vein,  West  Virginia 170 

Cole,  R.  A.,  sections  given  by 130, 192 

Columbia  mine,  Westmoreland  County, 

Pennsylvania,  section  at 68 

Coleman  limestone 93 

Columbiana  County,  Ohio,  section  in 131 

Colvin’s  Run,  Greene  County,  Pennsylva- 
nia, section  on 23 

Colvin’s  Run  limestone 89 

Conemaugh,  Pennsylvania,  section  at ... . 119 

Connellsville  sandstone 87 

Conoquenessing  sandstones 201 

Cook  vein,  West  Virginia 171 

Copeman’s  Knob,  West  Virginia,  section 

at 65 

Cove  Creek,  Wayne  County,  West  Vir- 
ginia, sections  on 155-156, 157 

Craig,  Geo.,  record  of  boring  furnished 

by 54 

Crane  Creek,  Mercer  County,  West  Vir- 
ginia, sections  on 198, 203 


Page. 


Cressov,  Pennsylvania,  section  at 122 

Crinoidal  coal 91,92 

Crinoidal  limestone 90-91 

Cucumber  Run,  Fayette  County,  Pennsyl- 
vania, section  on 116 

Current’s  farm,  Upshur  County,  West 

Virginia,  section  at 152 


D. 


Dickinson  Salt  Works,  West  Virginia, 

section  at 138 

Doubleday,  Mr.,  section  furnished  by 114 

Dunbar  Creek,  Fayette  County,  Pennsyl- 
vania, section  at 74 

Dunkard  coal 33-34 

Dunkard  Creek  beds,  fossils  of 41-42 

Dunkard  Creek,  Greene  County,  Pennsyl- 
vania, section  on 22 

Dunkard  Creek  series 19, 20^42 

highest  beds  of 30 

age  of 41-42 

Dunkard  Creek  series.  See  Permo-Car- 
boniferous. 


E. 

Eagle  limestone 141, 177 

Eagle,  West  Virginia,  section  at 176 

East  Brady,  Pennsylvania,  section  at 106 

Edwards,  W. S.,  sections  furnished  by...  136,195 

Elk  County,  Pennsylvania,  sections  in  ..  104, 182 

Elk  Lick  coal *. 89-90 

Elk  Lick  limestone 90 

Elk  River  series 70-98 

Elk  River,  West  Virginia,  section  at 

mouth  of - 136 

Epler  oil  boring,  Washington  County, 

Ohio,  section  at 192 


F. 


Fairfax,  Knob,  West  Virginia,  section  at.  65 

section  near 82 

Fall  Brook,  Pennsylvania,  section  at 103 

Farmington,  West  Virginia,  section  at...  37 

section  near 189 

Fayette  County,  Pennsylvania,  sections 

in 44,74,116 

Fayette  County,  West  Virginia 176, 197 

Federal  Creek,  Ohio,  section  at 67 

Ferriferous  limestone 173-175 

Fire  Creek  coal - 203 

Fish  Creek  sandstone 33 

Fishing  Creek,  Wetzel  County,  West 

Virginia,  section  on 38 

Fishpot  limestone  = Sewickley  limestone.  62 
Fleming,  Cochran,  records  of  borings  fur- 
nished by 73, 112 

Flipping  Creek,  West  Virginia,  section  on  204 

Fontaine,  W.  M.,  formation  named  by 179 

Fossil  horizons  and  localities 31,  34,  35,  37;  38, 

41,  42,  57,  59,  60,  62,  79,  90-91,  94, 
97,  98,  159, 163, 169, 177, 179-180 
Fossils  of  the  Upper  Coal  Measures 69 


Fossil  plant  horizons  and  localities  . - 34,  35, 37,  38, 

41,  42, 57, 97, 169, 179-180,  205 


INDEX. 


209 


Page. 

Fox  Township,  Elk  County,  Pennsylva- 
nia, section  in 182 

Freeport  coals 160-161 

Freeport  limestone 163 

Freeport,  Pennsylvania,  section  at Ill 

Freeport  sandstone 163-164 

Fulton,  John,  sections  given  by 118, 122 

Fulton  vein,  Pennsylvania  = Lower  Kit- 

tanningcoal 169 

G. 

Gallitzin  coal=Mahoning  coal  (?) 96 

Gallitzin,  Pennsylvania,  sections  near 148-149 

Gas  (natural)  first  used  for  manufacturing 
purposes  at  Burning  Spring,  "West 

Virginia 196 

Gilboy  sandstone =Browntown  sandstone  58 

Gilmer  County,  "West  Virginia,  section  in.  53 

Gilmore  sandstone 31 

Gladden’s  Run,  Pennsylvania,  section  on.  186 

Gray  Ore,  Ohio 173 

“Great”  Conglomerate =Pottsville  Con- 
glomerate   179 

“ Great  ” limestone 59-60 

Greene  County,  Pennsylvania,  sections 

in 22,23,24,45 

Green  Fossiliferous  limestone 90-91 

Guernsey  County,  Ohio,  section  in 83 

Guyandotte  Mountain,  West  Virginia,  sec- 
tion at 142 

Guyandotte  River,  West  Virginia,  sec- 
tions on - 155,204 

H. 

Hacker’s  Valley  post-office,  West  Vir- 
ginia, section  at 153 

Haggerty,  John,  sections  furnished  by  . . . 105-106 

Hanging  Rock,  Ohio,  section  at 193 

Harrison  County,  Ohio,  section  in 68 

Harrison  County,  West  Virginia,  sections 

in 48,49, 129,189 

Hartford  City,  W est Virginia,  section  at . . 53-54 

Hartley’s  bank,  near  Masontown,  West 

Virginia,  section  at 150 

Hobson  coal  = Washington  coal 37 

Hocking  Valley,  Ohio,  sections  in 133, 168 

Hog  Hollow  coal  = Middle  Kittanning 

coal , 166 

Holly  River,  West  Virginia,  section  on. ..  153 

Holmes  County,  Ohio,  section  in 191 

Homewood  sandstone 199 

Horton  Township,  Elk  County,  Pennsyl- 
vania, section  at 104 

Hostetter  coal _ 33 

Hotchkiss,  Jed,  section  given  by 204 

Houtzdale,  Pennsylvania,  section  near. . . 124 

Hukill,  E.  M.,  section  furnished  by 113 

Huntingdon  County,  Pennsylvania,  sec- 
tions in 125, 185 

Huntington,  West  Virginia,  sections  at  . . 66, 84 

section  near 158 

L 

Indiana  County,  Pennsylvania,  sections  in  115 

Irondale  limestone  and  ore 95 

Bull.  65 14 


Page. 

Iron  ore  in  the  Upper  Coal  Measures 57-58 

Ironton,  Ohio,  sections  near 135 

J. 

Jackson  County,  Ohio,  section  in 193 

Jackson  Furnace,  Jackson  County,  Ohio, 

section  near 193 

Jackson,  T.  M.,  sections  furnished  by 129, 189 

Jackson  Township,  Cambria  County, 

Penn  syl vania,  section  in 119 

Jefferson  County,  Ohio,  section  in 68 

Jefferson  County,  Pennsylvania,  section 

in 183 

Johnston,  John  L.,  section  furnished  by . . 49 

Johnstown  (Cement)  limestone 165-166 

Johnstown,  Pennsylvania,  section  at 118 

Jolly  town  coal 34 

Jollytown  limestone 34 

Jordan,  Col.,  record  of  boring  near  Charles- 
ton, West  Virginia,  furnished  by . . 137 

K. 

Kanawha  Black  Flint 98 

Kanawha  County,  West  Virginia,  sections 

in 85,136,138,162,195,196 

Karthaus,  Pennsylvania,  section  near 103 

Kellersburgh,  Pennsylvania,  section  at...  184 

Kenova,  West  Virginia,  section  near 158 

Kittanning  coals 164-165, 166-167, 169-170 

Kittanning  fire  clay 171 

Kittannin g,  Pennsylvania,  section  near. . . 109 

Kittanning  sandstone 172 

L. 

Laughlintown,  Pennsylvania,  section  near  116 

Laurel  Run,  Westmoreland  County,  Penn- 
sylvania, section  on 116 

Lawrence  County,  Kentucky,  sections  in  144, 145 

162-163, 194 

Leading  Creek,  Gilmer  County,  West  Vir- 
ginia, section  on 53 

Letonia,  Ohio,  section  near 132 

Lesley,  J.  P.,  Pottsville  conglomerate 

named  by 179 

Lewis  County,  West  Virginia,  section  in . 153 

Liberty  Township,  Washington  County, 

Ohio,  section  at 29 

Lick  Run,  West  Virginia,  section  at  mouth 

of 137 

Ligonier,  Pennsylvania,  section  at 75 

Limestone  Hill,  West  Virginia,  exposure 

of  limestone  at 33 

Limestone  ore,  Ohio 173 

Linton,  Prof.,  sections  given  by 113,185 

Little  Beaver  Creek,  Pennsylvania,  sec- 
tion at  mouth  of 130 

Little  Clarksburgh  coal 88 

Little  Falls,  West  Virginia,  section  at 80 

Little  Kanawha  River,  West  Virginia, 

section  on 153 

Little  Laurel  Creek,  West  Virginia,  sec- 
tion on 156 

Little  Pittsburgh  coal 88-87 


210 


INDEX, 


Page. 


Little  ‘Washington  coal 39 

Little  Waynesburg  coal 58 

Lloyd  Wamsley’s  bank,  Upshur  County, 

West  Virginia,  section  at 152 

Lockport,  Pennsylvania,  section  near 115 

Logansport,  Pennsylvania,  section  at 110 

Logan  County,  West  Virginia,  section  in.  147 
Lovejoy,  E.,  sections  in  Ohio  furnished  by  . 66, 67 

Lower  C am  bridge  limestone =Bru  sh  C reek 

limestone 93 

Lower  Cambridge  limestone=Philson 

limestone  94 

Lower  Carboniferous  beds 205 

Lower  Coal  Measures 19,  99-178 

Lower  Coal  Measures,  table  showing  strata 

of 101 

Lower  Freeport  coal 160-161 

Lower  Freeport  limestone 163 

Lower  Freeport  sandstone 163-164 

Lower  Kittanning  coal 169-170 

M. 

Mahoning  coal 96 

Mahoning  County,  Ohio,  section  in 191 

Mahoning  limestone 96-97 

Mahoning  River,  Ohio,  section  on 191 

Mahoning  sandstones 95-96,  97 

Malden,  West  Virginia,  section  near 138 

Maple  Swamp  water  tank,  West  Virginia 

Central  R.  R.,  section  at 127 

Mapletown  coal  = Sewickley  coal 61 

Marietta  sandstones 35-36 

Marion  County,  West  Virginia,  sections 

in 37,48,129,189 

Marshall  County,  West  Virginia,  sections 

in 25, 26 

Martin  County,  Kentucky,  section  in 146 

Mason  County,  West  Virginia,  sections  in.  54 

Masontown,  West  Virginia,  coal  bed  at..  94 

Masontown,  West  Virginia,  section  near.  150 

Massillon  sandstone  = Connoquenessing 

sandstones  in  part 201 

Mauch  Chunk  red  shale,  geologic  place  of.  19 

McCoy  shaft,  near  Gallitzin,  Cambria 

County,  Pennsylvania,  section  at.  148-149 

McCuneville,  Ohio,  section  near 133 

McDowell  County,  WestVirginia,  section 

in 203 

Meeker’s  Run,  Athens  County,  Ohio,  sec- 
tion on 134 

Mehaffey,  J.  A.,  section  on  Beaver  Run, 

Pennsylvania,  given  by 114 

Meigs  County,  Ohio,  sections  in 63,  66 

Meigs  Creek  coal  = Sewickley  coal 61 

Mercer  County,  Pennsylvania,  sections  in . 190 

Mercer  County,  West  Virginia,  sections 

in 198, 203, 204 

Mercer  group 200-201 

Middle  Cannelton  coal 97 

Middle  Freeport  coal 160 

Middle  Kittanning  coal 166-167 

Miller’s  Eddy,  Pennsylvania,  section  at..  105 

Mineral  County,  West  Virginia,  sections 

in 126, 127, 186 

Minshall,  F,  W.,  sections  furnished  by. . 29, 


52, 83, 192 


Page. 

Moatsville,  Barbour  County,  West  Vir- 
ginia, section  at 128 

Monongalia  County,  West  Virginia,  sec- 
tions in 38, 46, 47, 79,  80 

Monongahela  River  series 42-69 

Morgantown  sandstone 88-89 

Morgantown,  West  Virginia,  section  at  . . 79 

Morrisdale,  Pennsylvania,  section  near..  123 
Moundsville,  West  Virginia,  section  at. . . 51 

Mountain  limestone,  geologic  place  of 19 

Mount  Equity  mine,  Bedford  County, 

Pennsylvania 149 

Mount  Morris  limestone 39-40 

Mount  Vernon  furnace,  Ohio,  section  near  134 

Mumble-the-Peg  Creek,  Nicholas  County, 

West  Virginia,  section  on 154 

Murray  sville,  Pennsylvania,  sections 

at 114, 184-185 


Muskingum  County,  Ohio,  section  in 132 

N. 

Natural  gas  first  used  for  manufacturing 
purposes  at  Burning  Spring,  West 

Virginia 196 

Nelson ville,  Ohio,  section  near 134 

New  Bethlehem,  Pennsylvania,  section  at.  106 

Newburg,  West  Virginia,  sections  at 65,  81, 

117, 167, 170 

New  Lisbon,  Ohio,  section  near 132 

New  Martinsville,  West  Virginia,  section 

at 27 

New  River  coal  group 202-203 

New  Straitsville,  Ohio,  section  at 168 

Nicholas  County,  West  Virginia,  sections 

in 153,154 

Nineveh  coal 32 

Nineveh  limestone - 32-33 

Nineveh  sandstone 32 

Nuttallburg,  West  Virginia,  section  at. ..  197 

Nuzum’s  Mill,  Marion  County,  West  Vir- 
ginia, section  at 129 

O. 

Oceana,  West  Virginia,  section  at 143 

Ohio  County,  W est  Virginia,  sections  in . . 49, 130 

Ohio  Geological  Survey  reports  cited 28,  66, 

67,  68, 132, 134, 135, 161, 165,  168, 178, 191, 199 
Old  Peach  Orchard,  Lawrence  County, 

Kentucky,  section  at 145 

Oliphant,  F.  H.,  record  of  borings  given 

by '....144,145,194 

Ore  Hill  furnace,  section  near 107 

Orton,  Edward,  strata  named  by * 93 

beds  of  lower  coal  measures  traced 

across  Ohio  by 101 

cited  on  subdivision  of  Ferriferous 

limestone  in  Ohio 131 

sections  given  by 134, 135 

cited  on  Ohio  equivalent  of  Upper 

Kittaning 165 

cited  on  Ohio  coal  beds 158 

cited  on  geologic  equivalent  of  Upper 

Kittanning  in  Ohio 165 

cited  on  Middle  Kittanning  coal  in 

Ohio 167 

geologic  identifications  by 175 


INDEX. 


211 


P. 

Page. 

Panther  Hill,  Ohio,  section  at 134 

Parkersburg,  West  Virginia,  sections  at. . 130, 192 

Parsons,  James,  section  furnished  by 187 

Patton  station.  Clarion  County,  Pennsyl- 
vania   ,.  183 

Peach  Orchard  coal,  geologic  place  of 146 


Pennsylvania  Geological  Survey  reports 

cited. 29,  31, 37, 42, 44,  68,  74,  93,  94, 103,  104, 
105, 106,  107,  108, 116, 120,  121,  122,  123,  125, 
126, 149, 169, 173,182,183, 184, 185, 189, 190,205 


Permo-Carboniferous  or  Dunkard  Creek 

series 19,  20-42 

age  of 41-42 

Perry  County,  Ohio,  sections  in 133, 168 

Philippi,  West  Virginia,  section  at 161 

Philson  limestone  = Lower  Cambridge 

limestone 94 

Piedmont,  West  Virginia,  sections  at 126, 186 

Pine  Creek  limestone 93 

Pinkerton  Point,  Pennsylvania,  section  at  121 
Pipe  Creek,  Belmont  County,  Ohio,  sec- 
tion at 51 

Pittsburgh  coal 63-64 

Pittsburgh  coal  iron  ores 86 

Pittsburgh  limestones 87 

Pittsburgh,  Pennsylvania,  section  at 184 

Pittsburgh  region,  section  in 72 

Pittsburgh  sandstone 63 

Plant  horizons  and  localities,  34,  35,  37,  38,  41,  42, 
57,  97, 169, 179-180, 205 

Platt,  Franklin,  strata  named  by 90 

geologic  identifications  by 91 

sections  given  by 103, 120, 121, 122 

Platt,  Messrs.,  strata  named  by 63 

section  furnished  by 76 

geologic  identifications  by 89, 164 

cited  on  geologic  place  of  Johnstown 

Cement  limestone 166 

Platt,  Wm.  G.,  sections  given  by.. 104, 108, 115, 184 
Pocahontas,  West  Virginia,  section  near.  203 

Pocono  sandstone,  geologic  place  of 19 

Pomeroy,  Meigs  County,  Ohio,  section  at  66 
Porter’s  (Greene),  Twelve  Pole  Creek, 

West  Virginia,  section  at 158 

Posten’s  bank,  near  Mason  town,  West 

Virginia,  section  near 150 

Pottsville  Conglomerate  series 19, 179-205 

Pottsville  series,  structure  of 199 

Powell  Mountain,  West  Virginia,  section 

at....: 153 

Preston  County,  West  Virginia,  sections  in  65 
117, 150, 167, 170, 188 
Putnam  County,  West  Virginia, sections  in  55,  56 
Putneyville,  Pennsylvania,  section  at ....  108 

Q- 

Quakertown,  Ohio,  section  near 191 

Quakertown  coal 201 

Qainniinont  coal 203 

R. 

Raleigh  County,  West  Virginia,  section  in  142 
Randolph  County,  West  Virginia,  section 

in 151 


Page. 

Raymond  City,  West  Virginia 56 

Redstone  coal 62 

Redstone  limestone 62-63 

Red  shale  beds 92 

Rice’s  Landing,  Pennsylvania,  section  at.  45 

Richmond,  Pennsylvania,  section  near...  115 

“Ridge  ” limestone,  West  Virginia 33 

Ritchie  County,  West  Virginia,  section  in  159 
Roaring  Creek  coal  vein,  West  Virginia.  151 
Robinson’s  Run,  Monongalia  County, 

West  Virginia,  section  at 46 

Rock  Point  coal=Middle  Kittanning  coal  166 

Rogers  Brothers,  strata  named  by 70 

Rogers,  H.  D.,  strata  named  by 43, 59, 63, 147 

section  given  by 103 

Rogers’s  subdivision  of  the  Carboniferous  18-19 
Rowlesburg,  West  Virginia,  section  near  188 


S. 


Sawpit  branch  of  Cove  Creek,  West  Vir- 
ginia, section  on 157 

Scioto  County,  Ohio,  sections  in 134, 193 

Scott’s  Run,  Monongalia  County,  West 

Virginia,  section  at 47 

Scrub-grass  coal=Upper  Clarion  coal 175 

Selby,  A.  G.,  section  near  Huntington, 

West  Virginia,  furnished  by 84 

Serai  conglomerate=Pottsville  conglom- 
erate   179 

Sewickley  sandstone 60 

Sewickley  coal 60-61 

Sewickley  limestone 61-62 

Sewickley,  Pennsylvania,  sections  at .... . 73, 112 

Shade  Creek,  Ohio,  sections  at 66 

Sharon  coal 202 

Sharon  conglomerate 204-205 

Shawnee  limestone = Upper  Freeport...  159 

Shawnee,  Ohio,  section  near 133 

Shough’s  Knob,  Greene  County,  Pennsyl- 
vania, highest  Dunkard  beds  at..  130 
Shoup’s  Run,  Huntingdon  County,  Penn- 
sylvania, section  at 125 

Sbumard,  G.  F.,  section  furnished  by 145 

Simmons  Creek,  West  Virginia 203 

Simpson  well,  Wirt  County,  West  Vir- 
ginia, section 192 

Sims,  H.  N.,  section  given  by 125 

Somerset  County,  Pennsylvania,  sections 

in 121, 186 

South  Elk  Horn  Creek,  West  Virginia, 

section  on 203 

Sprucevale,  Ohio,  section  near 131 

Steele,  John  L.,  section  furnished  by 189 

Sterling  mines  near  Houtzdale,  Pennsyl- 
vania, section  at 124 

Steubenville,  Ohio,  section  at 77 

Stevenson,  John  J.,  strata  named  by 31,  32, 33 


34,  36, 37,  39,  59,  62,  88,  93 

sections  given  by 44,  68,74, 116, 126, 149, 159 

Stevenson,  Wm.  S.,  sections  given  by. . .78, 153, 185 
Stone  Coal  Run,  Upshur  County,  West 


Virginia,  section  at 161 

Stony  Creek,  Somerset  County,  Pennsyl- 
vania, soction  on 121 


212 


INDEX. 


Page. 


Stoyestown,  Pennsylvania,  section  at 121 

Stroud  Creek,  West  Virginia,  section  on. . 154 

Sugar  Camp  Hollo-w,  West  Virginia,  sec- 
tion in 157 

Summit  limestone=Mahoninglimestone.  96,  97 

Summit  limestone=Upper  Freeport 159 

T. 


Taylor  County,  ^ West  Virginia,  sectionsin.  128, 189 
Taylorstown,  Pennsylvania,  section  near.  30 

Thomas,  West  Virginia,  section  near 127 

Tioga  County,  Pennsylvania,  sections  in.  102,103 

Tionesta  coal= Upper  Mercer  coal 200-201 

Tipton  Bun  coals,  geologic  place  of 205 

Trimble  coal 167 

Trough  Creek,  West  Virginia, sections  on.  157 

Tucker  County,  West  Virginia,  sections 

on 65,  82, 127, 187 

Tug  Fork  of  Big  Sandy  Biver,  sections  on . 146, 147 
Twelve  Pole  Creek,  West  Virginia,  sec- 
tions on 156, 158 

Tygart’s  Valley  Biver,  section  on 128 

U. 

Uniontown  coal 59 

Uniontown  limestone 59 

Uniontown  sandstone 58-59 

Upper  Cannelton  coal 97 

Upper  coal  measures  or  Monongahela 

Biver  series 19, 42-69 

table  of  beds  of 57 

Upper  Freeport  coal 147-148 

Upper  Freeport  limestone 159 

Upper  Freeport  sandstone 160 

Upper  Kittanning  coal 164 

Upshur  County,  West  Virginia,  sections 

in 151, 152 

V. 

Valley  Falls,  West  Virginia,  section  at . . . 128 


W. 

Wall,  J.  Sutton,  section  near  Webster, 


Pennsylvania,  furnished  by 68 

Warfield  coal,  West  Virginia 171 

Warfield,  Kentucky,  section  at 146 

Washington  “A”  coal 35 

Washington  coal 37 


Washington  County,  Ohio,  sections  in. . .29, 52, 192 


Page 

Washington,  County,  Pennsylvania,  sec- 
tions in 29, 45,  78, 113, 185 

Washington  limestone.. 35,36 

Washington,  Pennsylvania,  sections  at. 29,  77-78 

113, 185 

Washington  sandstone..* 38-39 

Wayne  County,  West  Virginia,  sections  in.  155, 156 

157, 158 

Waynesburg  “A”  coal 39 

Waynesburg  “ B ” coal 39 

Waynesburg  coal 57 

Waynesburg  limestone 58 

Waynesburg  sandstone 40,  41 

Webster  County,  West  Virginia,  section  in  153 

Webster,  Pennsylvania,  section  near 68 

Wellersburg,  Pennsylvania,  section  near.  186 

Westernport  sandstone 59 

W eller  coal  = Crinoidal  coal 92 

Wellsburg,  West  Virginia,  section  at 190 

West  Brownsville,  Pennsylvania,  section 

at 45 

Westernport,  Maryland,  sections  near.. 56, 126, 186 
Westmoreland  County,  Pennsylvania,  sec- 
tions in 44,  68, 113, 114, 116, 185 

West  Virginia  Central  Bailroad,  sections 

on 127 

West  Virginia  and  Pittsburgh  Bailroad, 

section  on 152 

Wetzel  County,  West  Virginia,  sections  in  27,  38 
Wheeling  Creek,  Pennsylvania,  section  on  24 

Wheeling,  West  Virginia,  sections  at 130 

Willard,  E.  B.,  record  of  boring  furnished 

by 193 

Willey  fork  of  Fishing  Creek,  Wetzel 

County,  West  Virginia,  sections  on 38 

Wilson’s  mine,  Bandolph  County,  West 

Virginia,  section  at 151 

Windy  Gap  coal 31 

Windy  Gap  limestone 30-31 

Winfield,  West  Virginia,  section  at 55 

Winifrede,  West  Virginia,  sections  at 162 

Wirt  County,  West  Virginia,  sections  in  52,  83, 192 

Wise,  West  Virginia,  exposure  at 34 

Wood  County,  West  Virginia,  sections  in.  130, 192 

Wyoming  County,  West  Virginia,  sections 
in 143,204 

Z. 

Zanesville,  Ohio,  section  near 132 

Zoar  limestone  = Upper  Mercer  limestone  200 


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5 GEOLOGICAL  SURVEY 


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